Method for determination of pay saturation from seismic data

ABSTRACT

Methods for determination of pay saturation (S PAY ) and water saturation (S w ) from surface seismic data use amplitude changes with angle of incidence in conjunction with rock property relationships to determine pay saturation for a variety of situations. These situations include cases where P-P data is used and anisotropy and absorption are negligible; cases where P-P data is used and anisotropic effects are important; cases where contact events are evident; and cases where P-S data is used and anisotropy and absorption are negligible.

CROSS REFERENCE TO RELATED APPLICATIONS

This application claims the benefit of U.S. Provisional Application No. 60/100,033, filed Sep. 11, 1998.

BACKGROUND OF THE INVENTION

This invention relates generally to processing seismic trace data, and more specifically, it relates to methods for processing seismic trace data into estimations of hydrocarbon saturation. Existing methods for determining water saturation S_(w) or pay saturation S_(PAY) from seismic trace data is restricted to pre-stack isotropic P-P data. In addition, most existing methods make assumptions about the relationships between the rock properties for the reservoir. These assumptions limit either the accuracy or applicability of the technique.

SUMMARY OF THE INVENTION

The method of the present invention overcomes these problems with existing methods, by providing a methods which apply to pre-stack P-P data and to P-P angle stacked data for both the isotropic and, the more general, anisotropic case. In addition, the present invention provides a method for water and pay saturation determination from P-S data.

BRIEF DESCRIPTION OF THE DRAWINGS

FIG. 1 illustrates the AVO signature that results from using Equation 1.

FIG. 2 illustrates the AVO signature that results from using Equation 2.

FIG. 3 shows the density contrast Δρ as a function of the water saturation S_(w).

FIG. 4 shows the density contrast Δρ as a function of the water saturation S_(PAY).

FIG. 5 illustrates, for a pay fluid of gas, the sensitivity of the anisotropic parameter δ to S_(w), for various reasonable crack densities.

FIG. 6 illustrates, for a pay fluid of gas, the sensitivity of the anisotropic parameter δ to S_(PAY), for various reasonable crack densities.

FIG. 7 illustrates, for a pay fluid of gas, the sensitivity of the anisotropic parameter ε to S_(w), for various reasonable crack densities.

FIG. 8 illustrates, for a pay fluid of gas, the sensitivity of the anisotropic parameter δ to S_(PAY), for various reasonable crack densities.

FIG. 9 shows the geometry of a layer where the upper portion is a pay-filled reservoir (location A), a brine-filled portion of the reservoir (location B), and the contact event (location C).

FIG. 10 illustrates the OSA's behavior as a function of S_(w).

FIG. 11 shows the sensitivity of k_(f) to the water saturation S_(w).

FIG. 12 illustrates AVO signatures for g=2, of a density contrast and shear wave velocity contrast respectively.

FIGS. 13 and 14 show the accuracy of Equations 32 and 33, approximations to the Hudson equations.

DETAILED DESCRIPTION OF THE INVENTION

A number of methods will be outlined for determining hydrocarbon saturation from both P-P and P-S data. Each method will be applicable to areas and zones in which certain assumptions are satisfied. These assumptions, as well as the methods, will be described in some detail below.

Method 1

In the case where the cap rock and the reservoir are each isotropic, and the data type is P-P, the equations which describe the amplitude variation with offset and hence angle of incidence (θ), due to a reflection between the cap rock and reservoir, is given by:

AMP(θ)=A+B SIN²θ+C(TAN²θ−SIN²θ)  Equation 1

Where: $A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}$ $B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)} + {\frac{1}{2}\Delta \quad \delta}}$ $C = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\Delta \quad ɛ}}$

Or by:

AMP(θ)=B₀+B₁ TAN²θ+B₂ TAN²θ SIN²θ  Equation 2

Where: $B_{0} = {A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}}$ $B_{1} = {B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)}}}$ $B_{2} = {{C - B} = {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)}}$

Where: $g = \frac{\overset{\_}{Vp}}{\overset{\_}{Vs}}$ $\frac{\Delta \quad {Vp}}{\overset{\_}{Vp}} = \frac{{Vp}_{2} - {Vp}_{1}}{\overset{\_}{Vp}}$ $\frac{\Delta \quad {Vs}}{Vs} = \frac{{Vs}_{2} - {Vs}_{1}}{\overset{\_}{Vs}}$ $\frac{\Delta \quad \rho}{\rho} = \frac{\rho_{2} - \rho_{1}}{\overset{\_}{\rho}}$ $\overset{\_}{Vp} = \frac{{Vp}_{1} + {Vp}_{2}}{2}$ $\overset{\_}{Vs} = \frac{{Vs}_{1} + {Vs}_{2}}{2}$ $\overset{\_}{\rho} = \frac{\rho_{1} + \rho_{2}}{2}$

The subscript values 1 and 2, as in V_(p1) and V_(p2) should be interpreted as follows. “1” indicates the properties of the layer above the interface, while “2” indicates the properties of the layer below.

The rock property contrasts can be solved for in terms of the curve shape parameters. FIGS. 1 and 2 show the AVO (“amplitude versus offset”) signature that results from using Equations 1 and 2. Note the significance of the curve shape parameters A, B and C, or B₀, B₁ and B₂. $\begin{matrix} {\frac{\Delta \quad \rho}{\rho} = {2\left( {A - C} \right)}} & {{Equation}\quad 3} \\ {\frac{\Delta \quad {Vp}}{Vp} = {2C}} & {{Equation}\quad 4} \\ {{\frac{\Delta \quad {Vs}}{Vs} = {\left( {C - A} \right) + {\frac{g^{2}}{4}\left( {C - B} \right)}}}\text{Or:}} & {{Equation}\quad 5} \\ {\frac{\Delta \quad \rho}{\rho} = {2\left( {B_{0} - B_{1} - B_{2}} \right)}} & {{Equation}\quad 6} \\ {\frac{\Delta \quad {Vp}}{Vp} = {{2C} = {2\left( {B_{1} + B_{2}} \right)}}} & {{Equation}\quad 7} \\ {\frac{\Delta \quad {Vs}}{Vs} = {B_{0} - B_{1} - {B_{2}\left( {1 + \frac{g^{2}}{4}} \right)}}} & {{Equation}\quad 8} \end{matrix}$

The water saturation, S_(w) is given by: $\begin{matrix} {S_{w} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 9} \\ {S_{w} = \frac{2\left( {A - C} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 10} \end{matrix}$

Where:

A and C are the data derived curve fit coefficients;

Δρ is the density contrast between the cap rock and the pay filled reservoir;

ρ_(PAY) is the density of the pure pay fluid in situ;

ρ_(BR) is the density of the pure brine fluid in situ;

{overscore (ρ)} is the average density of the fluid filled reservoir and the shale cap rock; and

φ is the porosity of the reservoir.

The four parameters—ρ_(PAY), ρ_(BRINE), {overscore (ρ)}, φ—can be accurately estimated for a specific case.

FIG. 3 shows the density contrast Δρ as a function of the water saturation S_(w).

Finally, since:

S_(PAY)=1−S_(w)  Equation 11

Then: $\begin{matrix} {S_{PAY} = {1 - \frac{2\left( {A - C} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}} & {{Equation}\quad 12} \end{matrix}$

FIG. 4 shows the density contrast Δρ as a function of the pay saturation S_(PAY).

Or, in terms of B₀, B₁ and B₂: $\begin{matrix} {S_{w} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 13} \\ {S_{W} = \frac{2\left( {B_{0} - B_{1} - B_{2}} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 14} \end{matrix}$

Where:

B₀, B₁ and B₂ are the data derived curve fit coefficients;

Δρ is the density contrast between the cap rock and the pay filled reservoir;

ρ_(PAY) is an estimate of the density of pay fluid in situ;

ρ_(BR) is an estimate of the density of brine fluid in situ;

{overscore (ρ)} is an estimate of the average density of the fluid filled reservoir and the cap rock; and

φ is an estimate of the porosity of the reservoir.

The four parameters—ρ_(PAY), ρ_(BRINE), {overscore (ρ)}, φ—can be accurately estimated for a specific case.

Finally, using equation 11, then $\begin{matrix} {S_{PAY} = {1 - \frac{2\left( {B_{0} - B_{1} - B_{2}} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}} & {{Equation}\quad 15} \end{matrix}$

Method 2

The next method applies where either the cap rock or the reservoir, or both, are anisotropic. In that case, the equations which describe the amplitude variation with offset, and hence angle of incidence (θ) due to a reflection between the cap rock and the reservoir, is given by:

AMP(θ)=A+B SIN²θ+C (TAN²θ−SIN²θ)  Equation 16

Where: $A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}$ $B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)} + {\frac{1}{2}\Delta \quad \delta}}$ $C = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\Delta \quad ɛ}}$

Or by:

AMP(θ)=B₀+B₁ TAN²θ+B₂ TAN²θ SIN²θ  Equation 17

$B_{0} = {A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}}$ $B_{1} = {B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)} + {\frac{1}{2}\Delta \quad \delta}}}$ $B_{2} = {{C - B} = {{\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)} + {\frac{1}{2}\Delta \quad ɛ} - {\frac{1}{2}\Delta \quad \delta}}}$

Where: $g = \frac{\overset{\_}{Vp}}{\overset{\_}{Vs}}$ $\frac{\Delta \quad {Vp}}{\overset{\_}{Vp}} = \frac{{Vp}_{2} - {Vp}_{1}}{\overset{\_}{Vp}}$ $\frac{\Delta \quad {Vs}}{Vs} = \frac{{Vs}_{2} - {Vs}_{1}}{\overset{\_}{Vs}}$ $\frac{\Delta \quad \rho}{\rho} = \frac{\rho_{2} - \rho_{1}}{\overset{\_}{\rho}}$ Δ  δ = δ₂ − δ₁ Δ  ɛ = ɛ₂ − ɛ₁ $\overset{\_}{Vp} = {\frac{{Vp}_{1} + {Vp}_{2}}{2}{\overset{\_}{Vs} = {\frac{{Vs}_{1} + {Vs}_{2}}{2}{\overset{\_}{\rho} = \frac{\rho_{1} + \rho_{2}}{2}}}}}$

Where 1 indicates the properties for the layer above the interface while 2 indicates the layer below.

The rock property can be solved for in terms of the curve shape parameters A, B and C. $\begin{matrix} {\frac{\Delta \quad \rho}{\rho} = {{2\left( {A - C} \right)} + {\Delta \quad ɛ}}} & {{Equation}\quad 18} \\ {\frac{\Delta \quad V\quad \rho}{V\quad \rho} = {{2C} - {\Delta \quad ɛ}}} & {{Equation}\quad 19} \\ {\frac{\Delta \quad {Vs}}{Vs} = {\left( {C - A} \right) + {\frac{g^{2}}{4}\left( {C - B} \right)} + {\frac{g^{2}}{8}\left( {{\Delta \quad ɛ} - {\Delta \quad \delta}} \right)} + {\frac{1}{2}\Delta \quad ɛ}}} & {{Equation}\quad 20} \\ {{\Delta \quad ɛ} = {{2C} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}} & {{Equation}\quad 21} \\ {{\Delta \quad \delta} = {{\frac{8}{g^{2}} \cdot A} + {2 \cdot B} - {\left( {1 + \frac{4}{g^{2}}} \right)\quad \frac{d\quad V\quad \rho}{\overset{\_}{V\quad \rho}}} + \frac{8d\quad V_{s}}{V_{s}}}} & {{Equation}\quad 22} \end{matrix}$

The rock property can be solved for in terms of the curve shape parameters B₀, B₁ and B₂. $\begin{matrix} {\frac{\Delta \quad \rho}{\rho} = {{2\left( {B_{0} - B_{1} - B_{2}} \right)} + {\Delta \quad ɛ}}} & {{Equation}\quad 23} \\ {\frac{\Delta \quad V\quad \rho}{V\quad \rho} = {{2\left( {B_{1} + B_{2}} \right)} - {\Delta \quad ɛ}}} & {{Equation}\quad 24} \\ {\frac{\Delta \quad {Vs}}{Vs} = {B_{0} - B_{1} - {B_{2}\left( {1 + \frac{g^{2}}{4}} \right)} + {\frac{g^{2}}{g}\left( {{\Delta \quad ɛ} - {\Delta \quad \delta}} \right)} + {\frac{1}{2}\Delta \quad ɛ}}} & {{Equation}\quad 25} \\ {{\Delta \quad \delta} = {{\frac{8}{g^{2}}B_{0}} + {2B_{1}} - {\left( {1 + \frac{4}{g^{2}}} \right)\quad \frac{d\quad V\quad \rho}{\overset{\_}{V\quad \rho}}} + \frac{8d\quad V_{s}}{V_{s}}}} & {{Equation}\quad 26} \\ {{\Delta \quad ɛ} = {{2\left( {B_{1} + B_{2}} \right)} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}} & {{Equation}\quad 27} \end{matrix}$

The water saturation, S_(w) is given by the following derivation of equation 9: $\begin{matrix} {S_{w} = \frac{\left( {{2A} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 28} \end{matrix}$

Where:

A and C are the data derived curve fit coefficients;

ρ_(PAY) is the density of the pay fluid in situ;

ρ_(BR) is the density of brine fluid in situ;

{overscore (ρ)} is the average density of the fluid filled reservoir and the shale cap rock;

φ is the porosity of the reservoir; and $\frac{\Delta \quad {Vp}}{Vp}$

is the velocity contrast.

The five parameters—ρ_(PAY), ρ_(BRINE), {overscore (ρ)}, φ, $\frac{\Delta \quad {Vp}}{Vp}$

—can be accurately estimated.

The following equation for S_(PAY) is derived from equation 11: $\begin{matrix} {S_{PAY} = {1 - \frac{{2A} - \frac{\Delta \quad {Vp}}{Vp}}{\varphi\left( \left( {\rho_{BR} - \rho_{PAY}} \right) \right.}}} & {{Equation}\quad 29} \end{matrix}$

Or, in terms of B₀, B₁ and B₂, using equation 9, $\begin{matrix} {S_{w} = \frac{\left( {{2B_{0}} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 30} \end{matrix}$

Where:

B₀, B₁ and B₂ are the data derived curve fit coefficients;

ρ_(PAY) is an estimate of the density of pay fluid in situ;

ρ_(BR) is an estimate of the density of brine fluid in situ;

{overscore (ρ)} is an estimate of the average density of the fluid filled reservoir and the cap rock;

φ is an estimate of the porosity of the reservoir; and $\frac{\Delta \quad {Vp}}{Vp}$

is the velocity contrast.

The five parameters—ρ_(PAY), ρ_(BRINE), {overscore (ρ)}, φ, $\frac{\Delta \quad {Vp}}{Vp}$

—can be accurately estimated.

Using equation 11,

Then: $\begin{matrix} {S_{PAY} = {1 - \frac{{2B_{0}} - \frac{\Delta \quad {Vp}}{Vp}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}} & {{Equation}\quad 31} \end{matrix}$

A well known set of equations describes the relationships between the anisotropic parameters (δ and ε) and the crack density (e), and the incompressibility of the fluid filling the cracks. The equations are part of the Hudson anisotropic model. This model accurately represents the anisotropic behavior of a cracked medium filled with a fluid when the crack density is less than 0.1. Although very useful, the Hudson model equations are complicated and cannot be easily inverted to find the value of k_(f), which is the fluid incompressibility from values of δ and ε.

The Hudson equations apply only for small crack densities e, which is the norm in the subsurface. By making a series-expansion of the Hudson equation, but keeping only terms linear in e and not including products of e with any of the small parameters δ and ε, we get the following simplified relationships: $\begin{matrix} {ɛ = {ɛ_{intr} + \frac{8 \cdot e}{\left( {3 \cdot \left( {1 + {Kf}} \right)} \right)}}} & {{Equation}\quad 32} \\ {\delta = {\delta_{intr} + {\left( \frac{4 \cdot e}{1 + {Kf}} \right)\quad \left( {\frac{1}{3 \cdot \left( {g - 1} \right)} - \frac{1}{3 \cdot \left( {g + 1} \right)} + \frac{8}{3}} \right)} + \left( \frac{32 \cdot e}{3 \cdot \left( {2 - {3 \cdot g^{2}}} \right)} \right)}} & {{Equation}\quad 33} \\ \text{Or:} & \quad \\ {\delta = {\delta_{intr} + {e \cdot \left( {\frac{32}{\left( {9 \cdot \left( {1 + {Kf}} \right)} \right)} - \frac{16}{15}} \right)}}} & {{Equation}\quad 34} \end{matrix}$

Where ε_(intr) and δ_(intr) are the contributions due to the intrinsic anisotropy, which is the part not due to the presence of cracks. FIGS. 13 and 14 show the accuracy of Equations 32 and 33, approximations to the Hudson equations. The results of Equations 32 and 33 are marked “Linear” in FIGS. 13 and 14. The fluid incompressibility as a function of water saturation S_(w) can be written approximately as: $\begin{matrix} {k_{f} = \frac{k_{p} \cdot k_{b}}{k_{b} + {s_{w}\left( {k_{p} - k_{b}} \right)}}} & {{Equation}\quad 35} \end{matrix}$

Where:

k_(f) is the incompressibility of the composite fluid;

k_(b) is the incompressibility of the pure brine fluid; and

k_(p) is the incompressibility of the pure pay fluid.

 FIG. 11 shows the sensitivity of k_(f) to the water saturation S_(w).

By substituting Equation 34 into Equation 35, we get: $\begin{matrix} {ɛ = \frac{8 \cdot {e\left( {{S_{w}\left\lbrack {k_{p} - k_{b}} \right\rbrack} + k_{b}} \right)}}{3\left( {{k_{b}\left( {k_{p} + 1} \right)} + {S\left( {k_{p} - k_{b}} \right)}} \right)}} & {{Equation}\quad 36} \\ {{\Delta \quad ɛ} = {\frac{8 \cdot {e\left( {{S_{w}\left\lbrack {k_{p} - k_{b}} \right\rbrack} + k_{b}} \right)}}{3\left( {{k_{b}\left( {k_{p} + 1} \right)} + {S\left( {k_{p} - k_{b}} \right)}} \right)} + C}} & {{Equation}\quad 37} \end{matrix}$

Where C is a constant dependent on the anisotropy of the cap rock. For a pay fluid of gas, the sensitivity of the anisotropic parameter ε to S_(w) is shown in FIG. 7 for various reasonable crack densities. Note the excellent sensitivity of the parameter ε to S_(w). Solving for S_(w) we get: $\begin{matrix} {S_{w} \cong \frac{{8e} - {3{\left( {{\Delta \quad ɛ} - C} \right) \cdot \left( {1 + k_{p}} \right)}}}{\left( {{8e} - {3\left( {{\Delta \quad ɛ} - C} \right)}} \right) \cdot \left( {1 - \frac{k_{p}}{k}} \right)}} & {{Equation}\quad 38} \end{matrix}$

And S_(PAY) is given by: $\begin{matrix} {S_{PAY} \cong {\frac{3 \cdot \left( {{\Delta \quad ɛ} - C} \right) \cdot k_{p}}{\left( {1 - \frac{kp}{kb}} \right) \cdot \left( {{8e} - {3\left( {{\Delta \quad ɛ} - C} \right)}} \right)} - \frac{\frac{kp}{kb}}{1 - \frac{kp}{kb}}}} & {{Equation}\quad 39} \end{matrix}$

For a pay fluid of gas, the sensitivity of the anisotropic parameter ε to S_(PAY) is shown in FIG. 8 for various reasonable crack densities. Note the excellent sensitivity of the parameter to S_(PAY).

Next, by substituting Equation 35 into Equation 33, we get: $\begin{matrix} {\delta = {{\frac{\begin{matrix} {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} -} \right.}} \\ {\left. {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)} \right) \cdot \left( {{{kb} \cdot \left( {s - 1} \right)} - {{kp} \cdot s}} \right)} \end{matrix}}{\begin{matrix} {3 \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot} \\ {\left( {{3 \cdot g} - 2} \right) \cdot \left( {{{kb} \cdot \left( {{kp} - s + 1} \right)} + {{kp} \cdot s}} \right)} \end{matrix}}\text{Or:}}}} & {{Equation}\quad 40} \\ {{\Delta \quad \delta} = {{\frac{\begin{matrix} {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} -} \right.}} \\ {\left. {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)} \right) \cdot \left( {{{kb} \cdot \left( {s - 1} \right)} - {{kp} \cdot s}} \right)} \end{matrix}}{\begin{matrix} {3 \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot} \\ {\left( {{3 \cdot g} - 2} \right) \cdot \left( {{{kb} \cdot \left( {{kp} - s + 1} \right)} + {{kp} \cdot s}} \right)} \end{matrix}} + C}}} & {{Equation}\quad 41} \end{matrix}$

Where C is a constant dependent on the anisotropy of the cap rock. For a pay fluid of gas, the sensitivity of the anisotropic parameter δ to S_(w) is shown in FIG. 5 for various reasonable crack densities. Note the excellent sensitivity of the parameter to S_(w).

Solving for S_(w) we get: $\begin{matrix} {S_{w} \cong \frac{{\begin{matrix} {{kb} \cdot \left( {3 \cdot \left( {{\Delta \quad \delta} - C} \right) \cdot \left( {g - 1} \right) \cdot \left( {{kp} + 1} \right) \cdot} \right.} \\ {{\left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \\ {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} -} \right.}} \right.}} \end{matrix}}}{\begin{matrix} {\left( {{kb} - {kp}} \right) \cdot \left( {3 \cdot \left( {{\Delta \quad \delta} - C} \right) \cdot \left( {g - 1} \right) \cdot} \right.} \\ {{\left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \\ {8 \cdot e \cdot \left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} -} \right.}} \right.} \end{matrix}}} & {{Equation}\quad 42} \end{matrix}$

Or, if g≅2, by substituting Equation 53 into Equation 52, we get: $\begin{matrix} {{\delta = \frac{480 \cdot e \cdot \left( {{{kp} \cdot s} - {{kb} \cdot \left( {s - 1} \right)}} \right)}{{{kb} \cdot \left( {{135 \cdot {kp}} - {119 \cdot \left( {s - 1} \right)}} \right)} + {119 \cdot {kp} \cdot s}}}\text{And:}} & {{Equation}\quad 43} \\ {{\Delta \quad \delta} = {\frac{480 \cdot e \cdot \left( {{{kp} \cdot s} - {{kb} \cdot \left( {s - 1} \right)}} \right)}{{{kb} \cdot \left( {{135 \cdot {kp}} - {119 \cdot \left( {s - 1} \right)}} \right)} + {119 \cdot {kp} \cdot s}} + C}} & {{Equation}\quad 43.5} \end{matrix}$

Solving for S_(w) we get: $\begin{matrix} {S_{w} = \frac{{{kb} \cdot \left( {{\left( {{\Delta \quad \delta} - C} \right) \cdot 135 \cdot {kp}} + 119} \right)} - {480 \cdot e}}{\left( {{kb} - {kp}} \right) \cdot \left( {{119 \cdot \left( {{\Delta \quad \delta} - C} \right)} - {480 \cdot e}} \right)}} & {{Equation}\quad 44} \end{matrix}$

Using equation 11, we solve for S_(PAY). For a pay fluid of gas, the sensitivity of the anisotropic parameter δ to S_(PAY) is shown in FIG. 6 for various reasonable crack densities. Note the excellent sensitivity of the anisotropic parameter δ to S_(PAY).

Method 3

In a case where a contact event is detectable on P-P data for an isotropic reservoir, the fluid changes, but the frame does not, making the shear modulus contrast zero. In this case, the AVO equation becomes:

AMP=A +B SIN²θ+C(TAN²θ−SIN²θ)  Equation 45

$\begin{matrix} {{A = {{\frac{1}{2}\quad \frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\quad \frac{\Delta \quad \rho}{\rho}}}}{B = {\frac{1}{2}\quad \frac{\Delta \quad {Vp}}{Vp}}}{C = {\frac{1}{2}\quad \frac{\Delta \quad {Vp}}{Vp}}}\text{Or:}} & \quad \\ {{AMP} = {B_{0} + {B_{1}{TAN}^{2}\theta} + {B_{2}{TAN}^{2}\theta*{SIN}^{2}\theta}}} & {{Equation}\quad 46} \\ {{B_{0} = {{\frac{1}{2}\quad \frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\quad \frac{\Delta \quad \rho}{\rho}}}}{B_{1} = {\frac{1}{2}\quad \frac{\Delta \quad {Vp}}{Vp}}}{B_{2} = 0}} & \quad \end{matrix}$

Using the above gives: $\begin{matrix} {\frac{\Delta \quad \rho}{\rho} = {2\left( {A - B} \right)}} & {{Equation}\quad 47} \end{matrix}$

The water saturation in g is given by: $\begin{matrix} {S_{W} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 48} \\ {S_{w} = \frac{2\left( {A - B} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 49} \end{matrix}$

Where:

A and B are the data derived curve fit coefficients;

ρ_(PAY) is the density of pure pay in situ;

ρ_(BR) is the density of pure brine in situ;

{overscore (ρ)} is the average density if the brine and fluid filled reservoir; and

φ is the porosity of the reservoir.

The four parameters—ρ_(PAY), ρ_(BR), {overscore (ρ)}, φ—can be accurately estimated.

Using equation 11, then: $\begin{matrix} {S_{PAY} = {1 - \frac{2\left( {A - B} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}} & {{Equation}\quad 50} \end{matrix}$

If Equation 46 is used, then the density contrast becomes: $\begin{matrix} {{\frac{\Delta \quad \rho}{\rho} = {2\left( {B_{0} - B_{1}} \right)}}\text{but:}} & {{Equation}\quad 51} \\ {S_{w} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 52} \\ {S_{w} = \frac{2\left( {B_{0} - B_{1}} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 53} \end{matrix}$

Where:

B₀ and B₁ are the data derived curve fit coefficients;

ρ_(PAY) is the density of pure pay in situ;

ρ_(BR) is the density of pure brine in situ;

{overscore (ρ)} is the average density of the brine and fluid filled reservoir; and;

φ is the porosity of the reservoir.

The four of these parameters—ρ_(PAY), ρ_(BR), {overscore (ρ)}, φ—can be accurately estimated.

Using equation 11, $\begin{matrix} {S_{PAY} = {1 - \frac{2\left( {B_{0} - B_{1}} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}} & {{Equation}\quad 54} \end{matrix}$

Method 4

The next method uses the amplitudes from the angle stacks of seismic data to determine rock property contrasts, which in turn can be related to the water and pay saturation. The equations which describe the AVO response associated with a contrast in the rock properties are given by:

AMP(θ)=A+B TAN²θ+C(TAN²θ−SIN²θ)

Or:

AMP(θ)=B₀+B₁ TAN²θ+B₂ TAN²θ SIN²θ

The angle stack and ending angle θ_(e) of the data, from some starting angle θ_(s), can be calculated from either of the above equations to produce: ${{STACK}\left( {\theta_{s},\theta_{e}} \right)} = \frac{\int_{\theta_{s}}^{\theta_{e}}{{{AMP}(\theta)}{\theta}}}{\int_{\theta}^{\theta}{\theta}}$

This gives:

STACK(θ_(s), θ_(e))=A·f₁(θ_(s), θ_(e))+B·f₂(θ_(s), θ_(e))+C·f₃(θ_(s), θ_(e))  Equation 60

Where:

A, B and C are the AVO curve shape parameters

And:

f₁=1  Equation 61

$\begin{matrix} {f_{2} = {\frac{1}{2}\left\lbrack {1 - \left( {\frac{{SIN}\quad \left( \theta_{e} \right){COS}\quad \left( \theta_{e} \right)}{\left( {\theta_{e} - \theta_{s}} \right)} - \frac{{SIN}\quad \left( \theta_{s} \right){COS}\quad \left( \theta_{s} \right)}{\left( {\theta_{e} - \theta_{s}} \right)}} \right)} \right\rbrack}} & {{Equation}\quad 62} \\ \begin{matrix} {f_{3} = \quad {\frac{1}{2}\left\lbrack {{- 3} + \frac{{{TAN}\quad \left( \theta_{e} \right)} - {{TAN}\quad \left( \theta_{s} \right)}}{\left( {\theta_{e} - \theta_{s}} \right)} +} \right.}} \\ {\quad \left. \frac{{{SIN}\quad \left( \theta_{e} \right){COS}\quad \left( \theta_{e} \right)} - {{SIN}\quad \left( \theta_{s} \right){COS}\quad \left( \theta_{s} \right)}}{\left( {\theta_{e} - \theta_{s}} \right)} \right\rbrack} \end{matrix} & {{Equation}\quad 63} \end{matrix}$

Or:

STACK(θ_(s), θ_(e))=B₀·G₁(θ_(s), θ_(e))+B₁·G₂(θ_(s), θ_(e))+B₂·G₃(θ_(sT), θ_(e))  Equation 64

Where B₀, B₁ and B₂ are the AVO curve shape parameters.

G₁=1  Equation 65

$\begin{matrix} {G_{2} = \left\lbrack {{\frac{1}{\left( {\theta_{e} - \theta_{s}} \right)}\quad \left( {{{TAN}\quad \left( \theta_{e} \right)} - {{TAN}\quad \left( \theta_{s} \right)}} \right)} - 1} \right\rbrack} & {{Equation}\quad 66} \\ \begin{matrix} {G_{3} = \quad \left\lbrack {{- \frac{3}{2}} + {\left( \frac{1}{\left( {\theta_{e} - \theta_{s}} \right)} \right)\left( {{{TAN}\quad \theta_{e}} - {{TAN}\quad \theta_{s}}} \right)} +} \right.} \\ {\quad \left. {\frac{1}{2}\left( \frac{1}{\theta_{e} - \theta_{s}} \right)\quad \left( {{{SIN}\quad \theta_{e}{COS}\quad \theta_{e}} - {{SIN}\quad \theta_{s}{COS}\quad \theta_{s}}} \right)} \right\rbrack} \end{matrix} & {{Equation}\quad 67} \end{matrix}$

A collection of angle stack amplitudes STACK₁, STACK₂, . . . STACK_(N), and their corresponding starting and ending stack angles (θ_(s), θ_(e))₁, (θ_(s), θ_(e))₂, . . . (θ_(s), θ_(e))_(N), can be fitted to either Equation 60 or 64 depending on which type of fit parameters are desired—A, B and C, or B₀, B₁ and B₂, respectively. The result will be optimal values being generated for the fit parameters A, B and C, or B₀, B₁ and B₂. The basis functions for the fit will be f₁, f₂ and f₃ as given by Equations 61, 62 and 63, if the parameters A, B and C are used, or G₁, G₂, and G₃ as given by Equation 65, 66 and 67, if B₀, B₁ and B₂, respectively, are used.

In terms of the curve shape parameters A, B and C, the rock property contrasts are: $\begin{matrix} {{\Delta \quad \delta} = {{\frac{8}{g^{2}} \cdot A} + {2 \cdot B} - {\left( {1 + \frac{4}{g^{2}}} \right)\quad \frac{d\quad V\quad \rho}{\overset{\_}{V}\quad \rho}} + {\frac{8}{g^{2}}\quad \frac{d\quad V_{s}}{{\overset{\_}{V}}_{s}}}}} & {{Equation}\quad 68} \\ {{\Delta \quad ɛ} = {{2C} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}} & {{Equation}\quad 69} \\ {\frac{\Delta \quad \rho}{\rho} = {{2\left( {A - C} \right)} + {\Delta \quad ɛ}}} & {{Equation}\quad 70} \end{matrix}$

In terms of the curve shape parameters, B₀, B₁ and B₂, the rock property contrasts are: $\begin{matrix} {{\Delta \quad \delta} = {{\frac{8}{g^{2}}B_{0}} + {2B_{1}} - {\left( {1 + \frac{4}{g^{2}}} \right)\quad \frac{d\quad V\quad \rho}{\overset{\_}{V}\quad \rho}} + {\frac{8}{g^{2}}\quad \frac{d\quad V_{s}}{{\overset{\_}{V}}_{s}}}}} & {{Equation}\quad 71} \\ {{\Delta \quad ɛ} = {{2\left( {B_{1} + B_{2}} \right)} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}} & {{Equation}\quad 72} \\ {\frac{\Delta \quad \rho}{\rho} = {2\left( {B_{0} - B_{1} - B_{2}} \right)}} & {{Equation}\quad 73} \end{matrix}$

The water saturation S_(w) is given by: $\begin{matrix} {S_{w} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 74} \\ {S_{w} = \frac{\left( {{2A} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 75} \end{matrix}$

Where:

A and C are the data derived curve fit coefficients;

ρ_(PAY) is the density of the pay fluid in situ;

ρ_(BR) is the density of brine fluid in situ;

{overscore (ρ)} is the average density of the fluid filled reservoir and the shale cap rock;

φ is the porosity of the reservoir; and $\frac{\Delta \quad {Vp}}{Vp}$

is the velocity contrast.

The five parameters—ρ_(PAY), ρ_(BRINE), {overscore (ρ)}, φ, $\frac{\Delta \quad {Vp}}{Vp}$

—can be accurately estimated.

Using equation 11, $\begin{matrix} {S_{PAY} = {1 - \frac{{2A} - \frac{\Delta \quad {Vp}}{Vp}}{\varphi\left( \left( {\rho_{BR} - \rho_{BPAY}} \right) \right.}}} & {{Equation}\quad 76} \end{matrix}$

Or, using equation 9, in terms of B₀, B₁ and B₂: $\begin{matrix} {S_{w} = \frac{\left( {{2B_{0}} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 77} \end{matrix}$

Where:

B₀, B₁, and B₂ are the data derived curve fit coefficients;

ρ_(PAY) is an estimate of the density of pay fluid in situ;

ρ_(BR) is an estimate of the density of brine fluid in situ;

{overscore (ρ)} is an estimate of the average density of the fluid filled reservoir and the cap rock;

φ is an estimate of the porosity of the reservoir; and $\frac{\Delta \quad {Vp}}{Vp}$

is the velocity contrast.

The five parameters—ρ_(PAY), ρ_(BRINE), {overscore (ρ)}, φ, $\frac{\Delta \quad {Vp}}{Vp}$

—can be accurately estimated.

Using equation 11, $\begin{matrix} {\delta = {\delta_{intr} + {e \cdot \left( {\frac{32}{\left( {9 \cdot \left( {1 + {Kf}} \right)} \right)} - \frac{16}{15}} \right)}}} & {{Equation}\quad 81} \end{matrix}$

Where ε_(intr) and δ_(intr) are the contributions due to the intrinsic anisotropy—the part not due to the presence of cracks. The fluid incompressibility as a function of water saturation S_(w) can be written approximately as: $\begin{matrix} {k_{f} = \frac{k_{p} \cdot k_{b}}{k_{b} + {s_{w}\left( {k_{p} - k_{b}} \right)}}} & {{Equation}\quad 82} \end{matrix}$

Where:

k_(f) is the incompressibility of the composite fluid;

k_(b) is the incompressibility of the pure brine fluid; and

k_(p) is the incompressibility of the pure pay fluid.

Where, by substituting Equation 34 into Equation 35, we get: $\begin{matrix} {ɛ = \frac{8 \cdot {e\left( {{S_{w}\left\lbrack {k_{p} - k_{b}} \right\rbrack} + k_{b}} \right)}}{3\left( {{k_{b}\left( {k_{p} + 1} \right)} + {S\left( {k_{p} - k_{b}} \right)}} \right)}} & {{Equation}\quad 83} \\ {{\Delta \quad ɛ} = {\frac{8 \cdot {e\left( {{S_{w}\left\lbrack {k_{p} - k_{b}} \right\rbrack} + k_{b}} \right)}}{3\left( {{k_{b}\left( {k_{p} + 1} \right)} + {S\left( {k_{p} - k_{b}} \right)}} \right)} + C}} & {{Equation}\quad 84} \end{matrix}$

Where C is a constant dependent on the anisotropy of the cap rock.

Solving for S_(w) we get: $\begin{matrix} {S_{w} = \frac{{8\quad e} - {3{\left( {{\Delta \quad ɛ} - C} \right) \cdot \left( {1 + k_{p}} \right)}}}{\left( {{8\quad e} - {3\left( {{\Delta \quad ɛ} - C} \right)}} \right) \cdot \left( {1 - \frac{k_{p}}{k}} \right)}} & {{Equation}\quad 85} \end{matrix}$

And S_(PAY) is given by: $\begin{matrix} {S_{PAY} = {\frac{{3 \cdot \left( {{\Delta \quad ɛ} - C} \right) \cdot k}\quad p}{\left( {1 - \frac{k\quad p}{k\quad b}} \right) \cdot \left( {{8\quad e} - {3{\left( {\Delta \quad ɛ} \right) \cdot}}} \right)} - \frac{\frac{k\quad p}{k\quad b}}{1 - \frac{k\quad p}{k\quad b}}}} & {{Equation}\quad 86} \end{matrix}$

Next, by substituting Equation 35 into Equation 33, we get: $\begin{matrix} {\delta = \frac{\begin{matrix} {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} -} \right.}} \\ {\left. {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)} \right) \cdot \left( {{{kb} \cdot \left( {s - 1} \right)} - {{kp} \cdot s}} \right)} \end{matrix}}{\begin{matrix} {3 \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g} - 2} \right) \cdot} \\ \left( {{{kb} \cdot \left( {{kp} - s + 1} \right)} + {{kp} \cdot s}} \right) \end{matrix}}} & {{Equation}\quad 87} \\ {{\Delta \quad \delta} = {\frac{\begin{matrix} {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} -} \right.}} \\ {\left. {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)} \right) \cdot \left( {{{kb} \cdot \left( {s - 1} \right)} - {{kp} \cdot s}} \right)} \end{matrix}}{\begin{matrix} {3 \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g} - 2} \right) \cdot} \\ \left( {{{kb} \cdot \left( {{kp} - s + 1} \right)} + {{kp} \cdot s}} \right) \end{matrix}} + C}} & {{Equation}\quad 88} \end{matrix}$

Where C is a constant dependent on the anisotropy of the cap rock. Solving for S_(w) we get: $\begin{matrix} {S_{w} = {\frac{\begin{matrix} {k\quad {b \cdot \left( {{3 \cdot {\Delta\delta} \cdot \left( {g - 1} \right) \cdot \left( {{k\quad p} + 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.}} \\ \left. {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)}} \right) \end{matrix}}{\begin{matrix} {\left( {{k\quad b} - {k\quad p}} \right) \cdot \left( {{3 \cdot {\Delta\delta} \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.} \\ \left. {8 \cdot e \cdot \left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)} \right) \end{matrix}}}} & {{Equation}\quad 89} \end{matrix}$

Or, if g≅2, by substituting Equation 53 into Equation 52, we get: $\begin{matrix} {\delta = \frac{480 \cdot e \cdot \left( {{{kp} \cdot s} - {{kb} \cdot \left( {s - 1} \right)}} \right)}{{{kb} \cdot \left( {{135 \cdot {kp}} - {119 \cdot \left( {s - 1} \right)}} \right)} + {119 \cdot {kp} \cdot s}}} & {{Equation}\quad 90} \\ {{\Delta \quad \delta} = {\frac{480 \cdot e \cdot \left( {{{kps} \cdot s} - {kb}} \right) \cdot \left( {s - 1} \right)}{{{kb} \cdot \left( {{135 \cdot {kp}} - {119 \cdot \left( {s - 1} \right)}} \right)} + {119 \cdot {kp} \cdot s}} + C}} & {{Equation}\quad 90.5} \end{matrix}$

Solving for S_(w) we get: $\begin{matrix} {S_{w} = \frac{{k\quad {b \cdot \left( {{{\left( {{\Delta\delta} - C} \right) \cdot 135 \cdot k}\quad p} + 119} \right)}} - {480 \cdot e}}{\left( {{k\quad b} - {k\quad p}} \right) \cdot \left( {{119 \cdot \left( {{\Delta\delta} - C} \right)} - {480 \cdot e}} \right)}} & {{Equation}\quad 91} \end{matrix}$

Method 5

The next method uses the amplitudes from the angle stacks of seismic data to determine optimal stack attributes (OSA) by forming linear combinations and products of linear combinations of the angle stacks. These attributes are formed so that their values are strongly dependent on the water saturation S_(w) or the pay saturation S_(pay). These OSA attributes can be calculated for 2-D or 3-D data sets and displayed in 2-D or 3-D to highlight zones which are fully pay saturated, or to allow discrimination of partial versus fully saturated reservoirs. The ability to provide such discrimination is an essential and valuable part of the risk assessment of a prospect. To form the OSA it is necessary to start with the AVO equations:

AMP(θ)=A+B TAN²θ+C(TAN²θ−SIN²θ)

Or:

AMP(θ)=B₀+B₁ TAN²θ+B₂ TAN²θ SIN²θ

The angle stack and ending angle θ_(e) of the data, from some starting angle θ_(s), can be calculated from either of the above equations to produce: ${{STACK}\quad \left( {\theta_{s},\theta_{e}} \right)} = \frac{\int_{\theta_{s}}^{\theta_{e}}{{{AMP}(\theta)}\quad {\theta}}}{\int_{\theta}^{\theta}\quad {\theta}}$

This gives:

STACK(θ_(s), θ_(e))=A·f₁(θ_(s), θ_(e))+B·f₂(θ_(s), θ_(e))+C·f₃(θ_(s), θ_(e))  Equation 92

Where:

A, B and C are the AVO curve shape parameters

And: $\begin{matrix} {f_{1} = 1} & {{Equation}\quad 93} \\ {f_{2} = {\frac{1}{2}\left\lbrack {1 - \left( {\frac{{{SIN}\left( \theta_{e} \right)}{{COS}\left( \theta_{e} \right)}}{\left( {\theta_{e} - \theta_{s}} \right)} - \frac{{{SIN}\left( \theta_{s} \right)}{{COS}\left( \theta_{s} \right)}}{\left( {\theta_{e} - \theta_{s}} \right)}} \right)} \right\rbrack}} & {{Equation}\quad 94} \\ {f_{3} = {\frac{1}{2}\begin{bmatrix} {{- 3} + \frac{{{TAN}\left( \theta_{e} \right)} - {{TAN}\left( \theta_{s} \right)}}{\left( {\theta_{e} - \theta_{s}} \right)} +} \\ \frac{{{{SIN}\left( \theta_{e} \right)}{{COS}\left( \theta_{e} \right)}} - {{{SIN}\left( \theta_{s} \right)}{{COS}\left( \theta_{s} \right)}}}{\left( {\theta_{e} - \theta_{s}} \right)} \end{bmatrix}}} & {{Equation}\quad 95} \end{matrix}$

Or:

STACK(θ_(s), θ_(e))=B₀·G₁(θ_(s), θ_(e))+B₁·G₂(θ_(s), θ_(e))+B₂·G₃(θ_(sT), θ_(e))  Equation 96

Where B₀, B₁ and B₂ are the AVO curve shape parameters. $\begin{matrix} {G_{1} = 1} & {{Equation}\quad 97} \\ {G_{2} = \left\lbrack {{\frac{1}{\left( {\theta_{e} - \theta_{s}} \right)}\left( {{{TAN}\left( \theta_{e} \right)} - {{TAN}\left( \theta_{s} \right)}} \right)} - 1} \right\rbrack} & {{Equation}\quad 98} \\ {G_{3} = \begin{bmatrix} {{- \frac{3}{2}} + {\left( \frac{1}{\theta_{e} - \theta_{s}} \right)\left( {{{TAN}\quad \theta_{e}} - {{TAN}\quad \theta_{s}}} \right)} +} \\ {\frac{1}{2}\left( \frac{1}{\theta_{e} - \theta_{s}} \right)\left( {{{SIN}\quad \theta_{e}{COS}\quad \theta_{e}} - {{SIN}\quad \theta_{s}{COS}\quad \theta_{s}}} \right)} \end{bmatrix}} & {{Equation}\quad 99} \end{matrix}$

The amplitude of the angle stacks can be written for set specific values for θ_(s) and θ_(e) as: $\begin{matrix} {{{STACK}\quad \left( {\theta_{s},\theta_{e}} \right)} = {{\alpha_{1}\frac{\Delta \quad V\quad \rho}{V\quad \rho}} + {\alpha_{2}\frac{\Delta \quad V_{s}}{V_{s}}} + {\alpha_{3}\frac{\Delta \quad \rho}{\rho}} + {\alpha_{4}\Delta \quad \delta} + {\alpha_{5}\Delta \quad ɛ}}} & {{Equation}\quad 100} \end{matrix}$

Where a₁ . . . a₅ are contrasts determined by θ_(s) and θ_(e).

Linear combinations of angle stacks can be formed as follows: $\begin{matrix} {\sum\limits_{i = 1}\quad {C_{i}{{STACK}\left( {\theta_{s_{i}},\theta_{e_{i}}} \right)}}} & {{Equation}\quad 101} \end{matrix}$

And products of linear combinations of the angle stack can be formed as follows: $\begin{matrix} {= {\left( {\sum\limits_{i}{C_{i}{{STACK}\left( {\theta_{s_{i}},\theta_{e_{i}}} \right)}}} \right)\left( {\sum\limits_{j}{D_{j}{{STACK}\left( {\theta_{s_{j}},\theta_{e_{j}}} \right)}}} \right)}} & {{Equation}\quad 102} \end{matrix}$

Where:

C_(i) and D_(i) are constants;

θ_(s) _(i) is the starting angle;

θ_(e) _(i) is the ending angle;

φ_(s) _(i) is the starting angle; and

φ_(e) _(i) is the ending angle.

With proper choices of θ_(s), θ_(e), φ_(s), φ_(e) and C_(i) and D_(i), an angle stack attribute can be created which varies strongly with S_(w) or S_(PAY). An example of an optimal angle stack attribute (OSA) for the case of an anisotropic low impedance reservoir is:

 OSA=(STACK(30−45))−STACK(15−30))  Equation 103

$\begin{matrix} {{OSA} = {{.22}\left( {\frac{\Delta \quad g}{g} + {{.51}\frac{\Delta\rho}{\rho}} - {{.51}{\Delta\delta}} - {{.49}{\Delta ɛ}}} \right)}} & {{Equation}\quad 103.1} \end{matrix}$

This OSA's behavior as a function of S_(w) is given in FIG. 10. This type of attribute is an optimal stack attribute (OSA). Monitoring the value of this attribute from the brine to pay portion of the reservoir, and noting the optimal attribute change, allows prediction of the degree of pay saturation from seismic.

Method 6

The final method applies where P-S data is available which has been sorted into CCP (“common conversion point”) gathers after having been velocity corrected, and preprocessed so as to preserve amplitude information. Next, amplitudes are extracted from the data on a lobe or sample-by-sample basis. These amplitudes, along with the P-wave velocity function and S-wave velocity function derived from the data or from a shear wave estimation, can be fitted using Equation 104, which describes the behavior of the amplitude as a function of the P-wave incidence angle (θ).

Equation 104 represents the linearization of the exact P-S reflectivity equations. The form of the equation is important and unique because each of the two terms D₀ and D₁ represent the AVO signatures of a density contrast and shear wave velocity contrast respectively. These signatures for g=2 are shown in FIG. 12. Note these two functions form the basic functions for linearized AVO analysis. These rock property contrasts are the most useful for establishing rock property interpretation. Besides providing ${\frac{\Delta \quad \rho}{\rho}\quad {and}\quad \frac{\Delta \quad V_{s}}{V_{s}}},$

Equations 107 and 108 show the basis functions for density and shear wave velocity contrasts given by Equations 107 and 108 respectively.

The curve shape interpretation of these basic functions is noticeably different compared with the P-P case. The P-P AVO signature can be characterized by intercept (A or B₀) slope (B or B₁) and curvature (C and B or B₂ and B₁). In the P-S case the intercept is always zero and hence is not a meaningful parameter. FIG. 12 shows the shape of the two basic functions which are approximately up to 60 degrees. $\begin{matrix} \begin{matrix} {{{AMP\_ PS}(\theta)} = \quad {{D_{0}\left( {\frac{{SIN}\quad {\theta \left( {{2{SIN}^{2}\theta} - g^{2}} \right)}}{2g\sqrt{g^{2} - {{SIN}^{2}\theta}}} - \frac{{SIN}\quad \theta \quad {COS}\quad \theta}{g}} \right)} +}} \\ {\quad {D_{1}\left( {\frac{2{SIN}^{3}\theta}{g\sqrt{g^{2} - {{SIN}^{2}\theta}}} - \frac{2{SIN}\quad \theta \quad {COS}\quad \theta}{g}} \right)}} \end{matrix} & {{Equation}\quad 104} \end{matrix}$

Where: $\begin{matrix} {D_{0} = \frac{\Delta\rho}{\overset{\_}{\rho}}} & {{Equation}\quad 105} \\ {D_{1} = \frac{\Delta \quad {Vs}}{\overset{\_}{Vs}}} & {{Equation}\quad 106} \end{matrix}$

And g is an estimate of Vp/Vs found either directly from the data or by using Vp and Vs estimates. The resulting curve fit parameter is: $D_{0} = \frac{\Delta\rho}{\rho}$

And its basis function is: $\begin{matrix} \left( {\frac{{SIN}\quad {\theta \left( {{2{SIN}^{2}\theta} - g^{2}} \right)}}{2g\sqrt{g^{2} - {{SIN}^{2}\theta}}} - \frac{{SIN}\quad {\theta COS}\quad \theta}{g}} \right) & {{Equation}\quad 107} \\ {{And}\text{:}} & \quad \\ {D_{1} = \frac{\Delta \quad {Vs}}{Vs}} & \quad \end{matrix}$

The other curve fit parameter is: $\begin{matrix} \left( {\frac{2{SIN}^{3}\theta}{g\sqrt{g^{2} + {{SIN}^{2}\theta}}} - \frac{2{SIN}\quad {\theta COS}\quad \theta}{g}} \right) & {{Equation}\quad 108} \end{matrix}$

These can be used to determine the water saturation in the following way: $\begin{matrix} {S_{w} = \frac{{\Delta \quad \rho_{PS}} - {\Delta\rho}_{BR}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 109} \end{matrix}$

Where:

Δρ_(PS)=ρ_(PS)−ρ_(SHALE);

Δρ_(BS)=ρ_(BS)−ρ_(SHALE);

ρ_(FLUID)=Density of the fluid filling the pore space φ—the fluid has water saturation S_(w);

ρ_(BR)=Density of the brine;

ρ_(PAY)=Density of the pure pay;

φ=Porosity of the reservoir;

ρ_(PS)=Density of pay filled layer of saturation S_(w); and

ρ_(PS)=Density of brine filled layer.

The pay saturation can be determined by combining the information provided by determining D₀ at two locations A and B as shown in FIG. 9. FIG. 9 shows the geometry of a layer where the upper portion is a pay-filled reservoir (location A), a brine-filled portion of the reservoir (location B), and the contact event (location C).

This gives:

(D₀)_(A)·{overscore (ρ)}=Δρ_(PS)  Equation 110

(D₀)_(B)·ρ=Δρ_(BS)  Equation 111

Which produces:

Δρ_(PS)−Δρ_(BS)=(D₀ _(A) −D₀ _(B) ){overscore (ρ)}  Equation 112

Resulting in: $\begin{matrix} {S_{w} = \frac{\left( {D_{0_{A}} - D_{0_{B}}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & {{Equation}\quad 113} \\ {{And}\text{:}} & \quad \\ {S_{PAY} = {{1 - S_{w}} = {1 - \frac{\left( {D_{0_{B}} - D_{0_{A}}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}}} & {{Equation}\quad 114} \end{matrix}$

Where:

Δρ_(PS)=ρ_(PS)−ρ_(SHALE);

Δρ_(BS)=ρ_(BS)−ρ_(SHALE);

ρ_(FLUID)=Density of the fluid filling the pore space φ—the fluid has water saturation S_(w);

ρ_(BR)=Density of the brine;

ρ_(PAY)=Density of the pure pay;

φ=Porosity of the reservoir;

ρ_(PS)=Density of pay filled layer of saturation S_(w); and

ρ_(PS)=Density of brine filled layer.

In summary, what has been shown are the following methods to determine pay saturation (S_(PAY)) and water saturation (S_(w)) of subsurface layers, from surface seismic data.

1. A method to determine pay saturation (S_(PAY)) of subsurface isotropic layers for P-P data, comprising the following steps:

a) Positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint.

b) Generating seismic waves with said sources, and detecting and recording the amplitudes of seismic waves reflected by discontinuities in isotropic parameters of said strata for each source-detector pair.

c) Acquiring seismic data by using a collection of sources and a collection of receivers with the data acquired in either 2-D or 3-D to be sorted into common midpoint (CMP), also known as CDP, gathers which have a common midpoint or reflection point with varying offsets for each of the traces as represented in this ensemble of traces.

d) Providing amplitude corrections to the data to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons and emerging back at the surface and being received by hydrophone or geophone recording devices. These corrections can be of a deterministic or statistical or combined nature. These corrections will result in amplitudes which now are governed purely by rock property contrasts in the subsurface and by by their tuning effects.

e) Velocity correcting the data using hyperbolic or nonhyperbolic methods, the result of which will be to produce optimally flat events.

f) Extracting amplitudes for each horizon in either of two ways. The first is to find the zero crossings of the trace, then find the extrema value between the zero crossings. Those extrema values will then be assigned to each sample of the data between the zero crossings. This is the lobe method. The second method is to extract the amplitude sample-by-sample.

g) Calculating the angle of incidence (θ) by using the velocity function and the source receiver separations for each sample or lobe for each trace.

h) Fitting the extracted amplitudes using the above method along with the corresponding angles of incidence (θ), resulting in the optimal data derived fit parameters (the curve shape parameters) A, B and C if Equation 1 is used, or B₀, B₁ and B₂ if Equation 2 is used.

i) Extracting the rock property contrasts from the curve shaped parameters using Equations 3, 4 and 5 if A, B and C are used, or Equations 6, 7 and 8 if B₀, B₁ and B₂ are used.

j) By determining the density contrast using Equation 3 if A, B and C are used, or Equation 6 if B₀, B₁ and B₂ are used, along with Equation 9, the water saturation will be given by Equation 10 or Equation 14, respectively.

k) Calculating the pay saturation using Equation 11 and resulting in Equation 12 in the case of A, B and C, or resulting in Equation 15 in the case of B₀, B₁ and B₂.

2. A method to determine pay saturation (S_(PAY)) of subsurface anisotropic layers for P-P data, comprising the following steps:

a) Positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint.

b) Generating seismic waves with said sources, and detecting and recording the amplitudes of seismic waves reflected by discontinuities in anisotropic parameters of said strata for each source-detector pair.

c) Acquiring seismic data by using a collection of sources and a collection of receivers with the data acquired in either 2-D or 3-D to be sorted into common midpoint (CMP), also known as CDP, gathers which have a common midpoint or reflection point with varying offsets for each of the traces as represented in this ensemble of traces.

d) Providing amplitude corrections to the data to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons and emerging back at the surface and being received by hydrophone or geophone recording devices. These corrections can be of a deterministic or statistical or combined nature. These corrections will result in amplitudes which now are governed purely by rock property contrasts in the subsurface and by their tuning effects.

e) Velocity correcting the data using hyperbolic or nonhyperbolic methods, the result of which will be to produce optimally flat events.

f) Extracting amplitudes for each horizon in either of two ways. The first is to find the zero crossings of the trace, then find the extrema value between the zero crossings. Those extrema values will then be assigned to each sample of the data between the zero crossings. This is the lobe method. The second method is to extract the amplitude sample-by-sample.

g) Calculating the angle of incidence (θ) by using the velocity function and the source receiver separations for each sample or lobe for each trace.

h) Fitting the extracted amplitudes using the above method along with the corresponding angles of incidence (θ), resulting in the optimal data derived fit parameters (the curve shape parameters) A, B and C if Equation 16 is used, or B₀, B₁ and B₂ if Equation 17 is used.

i) Extracting the rock property contrasts from the curve shaped parameters using Equations 18, 19, 20, 21 and 22 if A, B and C are used, or Equations 23, 24, 25, 26 and 27 if B_(0, B) ₁ and B₂ are used.

This method provides four ways of calculating S_(w) and S_(PAY):

j) By determining the density contrast using Equation 18 if A, B and C are used, or Equation 23 if B₀, B₁ and B₂ are used, along with Equation 9, the S_(w) will be given by Equation 28 or Equation 30, respectively.

k) Calculating the S_(PAY) using Equation 11 results in Equation 29 in the case of A, B and C, or Equation 31 in the case of B₀, B₁ and B₂.

l) Using Equations 38 and 21, S_(w) can be found in the case where A, B and C are used. Equations 38 and 27 can be used when B₀, B₁ and B₂ are used.

m) Using Equations 39 and 21, S_(PAY) can be found in the case where A, B and C are used. Equations 39 and 27 can be used when B₀, B₁ and B₂ are used.

n) Using Equations 42 and 22, S_(w) can be found in terms of A, B and C, or Equations 42 and 26 can be used in the case where B₀, B₁ and B₂ are used.

o) Using Equations 11, 42 and 22, S_(PAY) can be found in terms of of A, B and C, or Equations 11, 42 and 26 can be used in the case where B₀, B₁ and B₂ are used.

p) Using Equations 44 and 22, S_(w) can be found in terms of A, B and C, or Equations 44 and 26 can be used in the case where B₀, B₁ and B₂ are used.

q) Using Equations 11, 44 and 22, S_(PAY) can be found in terms of A, B and C, or Equations 11, 44 and 26 can be used in the case where B₀, B₁ and B₂ are used.

3. A method to determine pay saturation (S_(PAY)) of subsurface layers when a contact event is evident within the layers, comprising the following steps:

a) Positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint.

b) Generating seismic waves with said sources, and detecting and recording the amplitudes of seismic waves reflected by discontinuities in isotropic parameters of said strata for each source-detector pair.

c) Acquiring seismic data by using a collection of sources and a collection of receivers with the data acquired in either 2-D or 3-D to be sorted into common midpoint (CMP), also known as CDP, gathers which have a common midpoint or reflection point with varying offsets for each of the traces as represented in this ensemble of traces.

d) Providing amplitude corrections to the data to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons and emerging back at the surface and being received by hydrophone or geophone recording devices. These corrections can be of a deterministic or statistical or combined nature. These corrections will result in amplitudes which now are governed purely by rock property contrasts in the subsurface and by their tuning effects.

e) Velocity correcting the data using hyperbolic or nonhyperbolic methods, the result of which will be to produce optimally flat events.

f) Extracting amplitudes for each horizon in either of two ways. The first is to find the zero crossings of the trace, then find the extrema value between the zero crossings. Those extrema values will then be assigned to each sample of the data between the zero crossings. This is the lobe method. The second method is to extract the amplitude sample-by-sample.

g) Calculating the angle of incidence (θ) by using the velocity function and the source receiver separations for each sample or lobe for each trace.

h) Fitting the amplitudes extracted from the contact events using Equations 45 or 46 resulting in the optimal data derived fit parameters-the curve shape parameters A, B and C, or B₀, B₁ and B₂, respectively.

i) Extracting the rock property contrasts from the curve shaped parameters described above using Equations 47 or 51.

j) Using the density contrast resulting from Equation 3, along with Equation 20, the water saturation can be calculated giving Equations 49 or 53.

k) Calculating the pay saturation gives Equations 50 or 54.

4. A method to determine pay saturation (S_(PAY)) of subsurface isotropic or anisotropic layers for P-P data, comprising the following steps:

a) Positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint.

b) Generating seismic waves with said sources, and detecting and recording the amplitudes of seismic waves reflected by discontinuities in isotropic parameters of said strata for each source-detector pair.

c) Acquiring seismic data by using a collection of sources and a collection of receivers with the data acquired in either 2-D or 3-D to be sorted into common midpoint (CMP), also known as CDP, gathers which have a common midpoint or reflection point with varying offsets for each of the traces as represented in this ensemble of traces.

d) Providing amplitude corrections to the data to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons and emerging back at the surface and being received by hydrophone or geophone recording devices. These corrections can be of a deterministic or statistical or combined nature. These corrections will result in amplitudes which now are governed purely by rock property contrasts in the subsurface and by their tuning effects.

e) Velocity correcting the data using hyperbolic or nonhyperbolic methods, the result of which will be to produce optimally flat events.

f) Calculating the angle of incidence (θ) by using the velocity function and the source receiver separations for each sample or lobe for each trace.

g) Angle stacking of the data through various angle ranges θ_(s) and θ_(e).

h) Extracting amplitudes for each horizon from each angle stack in either of two ways. The first is to find the zero crossings of the trace, then find the extrema value between the zero crossings. Those extrema values will then be assigned to each sample of the data between the zero crossings. This is the lobe method. The second method is to extract the amplitude sample-by-sample.

i) Fitting the extracted angle stack amplitudes using the above method, resulting in the optimal data derived fit parameters (the curve shape parameter) A, B and C, or B₀, B₁ and B₂ using Equation 60 or 64.

j) Extracting the rock property contrasts from the curve shaped parameters using Equations 68, 69 and 70 if A, B and C are used, or Equations 71, 72 and 73 if B₀, B₁ and B₂ are used.

k) Using the density contrast resulting from Equation 70 or 73, along with Equation 20, the water saturation can be calculated giving Equations 75 or 77.

l) Calculating the pay saturation using Equation 11 gives Equations 76 and 78.

This method provides three ways of calculating S_(w) and S_(PAY).

m) By determining the density contrast using Equation 70 if A, B and C are used, or Equation 73 if B₀, B₁ and B₂ are used, along with Equation 9, the water saturation will be given by Equation 75 or Equation 77, respectively.

n) Calculating the pay saturation using Equation 11 results in Equation 76 in the case of A, B and C, or Equation 78 in the case of B₀, B₁ and B₂.

o) Using Equations 85 and 69, S_(w) can be found in the case where A, B and C are used. Equations 85 and 72 can be used when B₀, B₁ and B₂ are used.

p) Using Equations 86 and 69, S_(PAY) can be found in the case where A, B and C are used. Equations 86 and 72 can be used when B₀, B₁ and B₂ are used.

q) Using Equations 89 and 68, S_(w) can be found in terms of A, B and C, or Equations 89 and 71 can be used in the case where B₀, B₁ and B₂ are used.

r) Using Equations 89, 11 and 68, S_(PAY) can be found in terms of of A, B and C, or Equations 89, 11 and 71 can be used in the case where B₀, B₁ and B₂ are used.

s) Using Equations 91 and 68, S_(w) can be found in terms of A, B and C, or Equations 91 and 71 can be used in the case where B₀, B₁ and B₂ are used.

t) Using Equations 91, 11 and 68, S_(PAY) can be found in terms of of A, B and C, or Equations 91, 11 and 71 can be used in the case where B₀, B₁ and B₂ are used.

5. A method to determine pay saturation (S_(PAY)) of subsurface anisotropic or isotropic layers for P-P data, comprising the following steps:

a) Positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint.

b) Generating seismic waves with said sources, and detecting and recording the amplitudes of seismic waves reflected by discontinuities in isotropic parameters of said strata for each source-detector pair.

c) Acquiring seismic data by using a collection of sources and a collection of receivers with the data acquired in either 2-D or 3-D to be sorted into common midpoint (CMP), also known as CDP, gathers which have a common midpoint or reflection point with varying offsets for each of the traces as represented in this ensemble of traces.

d) Providing amplitude corrections to the data to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons and emerging back at the surface and being received by hydrophone or geophone recording devices. These corrections can be of a deterministic or statistical or combined nature. These corrections will result in amplitudes which now are governed purely by rock property contrasts in the subsurface and by their tuning effects.

e) Velocity correcting the data using hyperbolic or nonhyperbolic methods, the result of which will be to produce optimally flat events.

f) Calculating the angle of incidence (θ) to be determined using the velocity function and the source receiver separations for each sample or lobe for each trace.

g) Angle stacking of the data through various angle ranges, θ_(s) and θ_(e), will be performed.

h) Extracting amplitudes from the angle stacks for each horizon in either of two ways. The first is to find the zero crossings of the trace, then find the extrema value between the zero crossings. Those extrema values will then be assigned to each sample of the data between the zero crossings. This is the lobe method. The second method is to extract the amplitude sample-by-sample.

i) Generating the OSA by making linear combinations of the angle stacks or products of linear combinations using Equations 101 and 102, or products of linear combinations of the angle stacks, so as to generate a quantity which is strongly sensitive to the value of the water saturation S_(w), or pay saturation S_(PAY). See FIG. 10. Using Equations 92 or 96 and 100, establish relationships between the OSA's and rock property contrasts.

j) Using Equations 74, 84, 88 and other well known relationships, relating the rock property contrasts to the water saturation, S_(w), and pay saturation, S_(PAY).

k) Relating the water saturation, S_(w), and pay saturation, S_(PAY), using Equation 100 and the relationships from item “k.”

l) Displaying the OSA attributes in 2-D or 3-D and using them as a discriminating tool to find fully saturated layers and allowing the avoidance of low pay saturation layers.

6. A method to determine pay saturation (S_(PAY)) of subsurface layers for P-S data, comprising the following steps:

a) Positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint.

b) Generating seismic waves with said sources, and detecting and recording the amplitudes of seismic waves reflected by discontinuities in isotropic, anisotropic or absorption parameters of said strata for each source-detector pair.

c) Acquiring seismic data by using a collection of sources and a collection of receivers with the data acquired in either 2-D or 3-D to be sorted into common reflection point (CRP), gathers which have a common reflection point with varying offsets for each of the traces as represented in this ensemble of traces.

d) Providing amplitude corrections to the data to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons and emerging back at the surface and being received by hydrophone or geophone recording devices. These corrections can be of a deterministic, statistical or combined nature. These corrections will result in amplitudes which now are governed purely by rock property contrasts in the subsurface and by their tuning effects.

e) Velocity correcting the data using hyperbolic or nonhyperbolic methods, the result of which will be to produce optimally flat events.

f) Extracting amplitudes for each horizon in either of two ways. The first is to find the zero crossings of the trace, then find the extrema value between the zero crossings. Those extrema values will then be assigned to each sample of the data between the zero crossings. This is the lobe method. The second method is to extract the amplitude sample-by-sample.

g) Calculating the angle of incidence (θ) to be determined using the velocity function and the source receiver separations for each sample or lobe for each trace.

h) Fitting the extracted amplitudes using the above method resulting in the optimal data derived fit parameters (the curve shape parameter) DO and Di using Equation 104.

i) Extracting the rock property contrasts from the curve shaped parameters described above using Equations 105 and 106.

j) Using the density contrast resulting from Equations 105 and 106, along with Equation 109, to calculate the water saturation giving Equation 113.

k) Calculating the pay saturation using Equation 114.

7. A method to determine pay saturation (S_(PAY)) of subsurface isotropic layers for P-P data, comprising the following steps:

a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint;

b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface isotropic layers, for each source-detector pair;

c) sorting the traces into common midpoint (CMP) gathers, which have a common midpoint or reflection point, and have varying offsets;

d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons;

e) modifying the seismic data samples to generate velocity-corrected seismic data samples;

f) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted amplitudes;

g) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample;

h) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equation,

AMP(θ)=A+B SIN²θ+C(TAN²θ−SIN²θ)

where: $A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta\rho}{\rho}}}$ $B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta\rho}{\rho}} \right)} + {\frac{1}{2}{\Delta\delta}}}$ $C = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}{\Delta ɛ}}}$

to generate curve shape parameters A, B and C;

i) extracting rock property contrasts from the curve shape parameters using the following equations, $\frac{\Delta\rho}{\rho} = {2\left( {A - C} \right)}$ $\frac{\Delta \quad {Vp}}{Vp} = {2C}$ ${\frac{\Delta \quad {Vs}}{Vs} = {\left( {C - A} \right) + {\frac{g^{2}}{4}\left( {C - B} \right)}}};$

j) determining the density contrast using the following equation, $S_{w} = \frac{\Delta\rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}$

determining the water saturation by the following equation, ${S_{w} = \frac{2\left( {A - C} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}};{and}$

k) calculating the pay saturation using the following equations: $S_{PAY} = {{1 - {S_{w}\quad {and}\quad S_{PAY}}} = {1 - \frac{2\left( {A - C} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}}$

8. A method to determine pay saturation (S_(PAY)) of subsurface isotropic layers for P-P data, comprising the following steps:

a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint;

b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface isotropic layers, for each source-detector pair;

c) sorting the traces into common midpoint (CMP) gathers, which have a common midpoint or reflection point, and have varying offsets;

d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons;

e) modifying the seismic data samples to generate velocity-corrected seismic data samples;

f) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted amplitudes;

g) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample;

h) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equation,

AMP(θ)=B₀+B₁ TAN²θ+B₂ TAN²θ SIN ²θ

Where: $B_{0} = {A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}}$ $B_{1} = {B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta\rho}{\rho}} \right)}}}$ $B_{2} = {{C - B} = {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)}}$

Where: $g = \frac{\overset{\_}{Vp}}{\overset{\_}{\overset{\_}{Vs}}}$ $\frac{\Delta \quad {Vp}}{\overset{\_}{Vp}} = \frac{{Vp}_{2} - {Vp}_{1}}{\overset{\_}{Vp}}$ $\frac{\Delta \quad {Vs}}{Vs} = \frac{{Vs}_{2} - {Vs}_{1}}{\overset{\_}{Vs}}$ $\frac{\Delta\rho}{\rho} = \frac{\rho_{2} - \rho_{1}}{\overset{\_}{\rho}}$ $\overset{\_}{Vp} = \frac{{Vp}_{1} + {Vp}_{2}}{2}$ $\overset{\_}{Vs} = \frac{{Vs}_{1} + {Vs}_{2}}{2}$ $\overset{\_}{\rho} = \frac{\rho_{1} + \rho_{2}}{2}$

i) to generate curve shape parameters B₀, B₁ and B₂;

j) extracting rock property contrasts from the curve shape parameters using the following equations, Equations 6, 7 and 8 if B₀, B₁ and B₂ are used $\frac{\Delta\rho}{\rho} = {2\left( {B_{0} - B_{1} - B_{2}} \right)}$ $\frac{\Delta \quad {Vp}}{Vp} = {{2C} = {2\left( {B_{1} + B_{2}} \right)}}$ $\frac{\Delta \quad {Vs}}{Vs} = {B_{0} - B_{1} - {B_{2}\left( {1 + \frac{g^{2}}{4}} \right)}}$

determining the density contrast using the following equation, $S_{w} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}$

k) determining the water saturation by the following equation, ${S_{W} = \frac{2\left( {B_{0} - B_{1} - B_{2}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}};{and}$

l) calculating the pay saturation using the following equations: $S_{PAY} = {{1 - {S_{w}\quad {and}\quad S_{PAY}}} = {1 - \frac{2\left( {B_{0} - B_{1} - B_{2}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}}}$

Although this detailed description has shown and described illustrative embodiments of the invention, this description contemplates a wide range of modifications, changes, and substitutions. In some instances, one may employ some features of the present invention without a corresponding use of the other features. Accordingly, it is appropriate that readers should construe the appended claims broadly, and in a manner consistent with the scope of the invention. 

What is claimed is:
 1. A method to determine pay saturation (S_(PAY)) of subsurface isotropic layers for P-P data, comprising the following steps: a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint; b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface isotropic layers, for each source-detector pair; c) sorting the traces into common midpoint (CMP) gathers, which have a common midpoint or reflection point, and have varying offsets; d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons; e) modifying the seismic data samples to generate velocity-corrected seismic data samples; f) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted amplitudes; g) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample; h) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equation, AMP(θ)=A+B SIN²θ+C(TAN²θSIN²θ)  where: $A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}$ $B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)} + {\frac{1}{2}\Delta \quad \delta}}$ $C = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\Delta \quad ɛ}}$

 to generate curve shape parameters A, B and C; i) extracting rock property contrasts from the curve shape parameters using the following equations, $\frac{\Delta \quad \rho}{\rho} = {2\left( {A - C} \right)}$ $\frac{\Delta \quad {Vp}}{Vp} = {2C}$ ${\frac{\Delta \quad {Vs}}{Vs} = {\left( {C - A} \right) + {\frac{g^{2}}{4}\left( {C - B} \right)}}};$

j) determining the density contrast using the following equation, $S_{w} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}$

 determining the water saturation by the following equation, ${S_{w} = \frac{2\left( {A - C} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}};\quad {and}$

k) calculating the pay saturation using the following equations: $S_{PAY} = {{1 - {S_{w}\quad {and}\quad S_{PAY}}} = {1 - {\frac{2\left( {A - C} \right)\quad \overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}}}$


2. A method to determine pay saturation (S_(PAY)) of subsurface isotropic layers for P-P data, comprising the following steps: a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint; b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface isotropic layers, for each source-detector pair; c) sorting the traces into common midpoint (CMP) gathers, which have a common midpoint or reflection point, and have varying offsets; d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons; e) modifying the seismic data samples to generate velocity-corrected seismic data samples; f) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted amplitudes; g) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample; h) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equation, AMP(θ)=B₀+B₁ TAN²θ, B₂ TAN²θ SIN²θ  Where: $B_{0} = {A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}}$ $B_{1} = {B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta\rho}{\rho}} \right)}}}$ $B_{2} = {{C - B} = {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)}}$

 Where: $g = \frac{\overset{\_}{Vp}}{\overset{\_}{\overset{\_}{Vs}}}$ $\frac{\Delta \quad {Vp}}{\overset{\_}{Vp}} = \frac{{Vp}_{2} - {Vp}_{1}}{\overset{\_}{Vp}}$ $\frac{\Delta \quad {Vs}}{Vs} = \frac{{Vs}_{2} - {Vs}_{1}}{\overset{\_}{Vs}}$ $\frac{\Delta\rho}{\rho} = \frac{\rho_{2} - \rho_{1}}{\overset{\_}{\rho}}$ $\overset{\_}{Vp} = \frac{{Vp}_{1} + {Vp}_{2}}{2}$ $\overset{\_}{Vs} = \frac{{Vs}_{1} + {Vs}_{2}}{2}$ $\overset{\_}{\rho} = \frac{\rho_{1} + \rho_{2}}{2}$

i) to generate curve shape parameters B₀, B₁ and B₂; j) extracting rock property contrasts from the curve shape parameters using the following equations, $\frac{\Delta\rho}{\rho} = {2\left( {B_{0} - B_{1} - B_{2}} \right)}$ $\frac{\Delta \quad {Vp}}{Vp} = {{2C} = {2\left( {B_{1} + B_{2}} \right)}}$ $\frac{\Delta \quad {Vs}}{Vs} = {B_{0} - B_{1} - {B_{2}\left( {1 + \frac{g^{2}}{4}} \right)}}$

 determining the density contrast using the following equation, $S_{w} = \frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}$

k) determining the water saturation by the following equation, ${S_{W} = \frac{2\left( {B_{0} - B_{1} - B_{2}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}};{and}$

l) calculating the pay saturation using the following equations: $S_{PAY} = {{1 - {S_{w}\quad {and}\quad S_{PAY}}} = {1 - {\frac{2\left( {B_{0} - B_{1} - B_{2}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}}}$


3. A method for determining pay saturation (S_(PAY)) of subsurface anisotropic layers for P-P data, comprising the following steps: a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint; b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface anisotropic layers, for each source-detector pair; c) sorting the traces into common midpoint (CMP) gathers, which have a common midpoint or reflection point, and have varying offsets; d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons; e) modifying the seismic data samples to generate velocity-corrected seismic data samples; f) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted amplitudes; and g) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample.
 4. The method of claim 3, further comprising the steps of: a) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equation, AMP(θ)=A+B SIN²θ+C(TAN²θ−SIN²θ)  Where: $A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta\rho}{\rho}}}$ $B = {{\frac{1}{2}\frac{\Delta \quad {VP}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta\rho}{\rho}} \right)} + {\frac{1}{2}{\Delta\delta}}}$ $C = {{\frac{1}{2}\frac{\Delta \quad {VP}}{Vp}} + {\frac{1}{2}{\Delta ɛ}}}$

 to generate curve shape parameters A, B and C; and b) extracting rock property contrasts from the curve shape parameters using the following equations, $\frac{\Delta\rho}{\rho} = {{2\left( {A - C} \right)} + {\Delta ɛ}}$ $\frac{\Delta \quad V\quad \rho}{V\quad \rho} = {{2C} - {\Delta ɛ}}$ $\frac{\Delta \quad {Vs}}{Vs} = {\left( {C - A} \right) + {\frac{g^{2}}{4}\left( {C - B} \right)} + {\frac{g^{2}}{8}\left( {{\Delta ɛ} - {\Delta\delta}} \right)} + {\frac{1}{2}{\Delta ɛ}}}$ ${\Delta ɛ} = {{2C} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}$ ${\Delta\delta} = {{\frac{8}{g^{2}} \cdot A} + {2 \cdot B} - {\left( {1 + \frac{4}{g^{2}}} \right)\frac{{dV}\quad \rho}{\overset{\_}{V\quad \rho}}} + {\frac{8{dV}_{s}}{V_{s}}.}}$


5. The method of claim 4, further comprising the steps of: a) determining the water saturation by the following equation, ${S_{w} = \frac{\left( {{2A} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}};$

 where: A and C are the data derived curve fit coefficients; ρ_(PAY) is the density of the pay fluid in situ; ρ_(BR) is the density of brine fluid in situ; {overscore (ρ)} is the average density of the fluid filled reservoir and the shale cap rock; φ is the porosity of the reservoir; and $\frac{\Delta \quad {Vp}}{Vp}$

is the velocity contrast, and b) calculating the pay saturation using the following equation: $S_{PAY} = {1 - {\frac{{2A} - \frac{\Delta \quad {Vp}}{Vp}}{\varphi\left( \left( {\rho_{BR} - \rho_{BPAY}} \right) \right.}.}}$


6. The method of claim 4, further comprising the steps of: a) determining the water saturation by the following equations, $S_{w} \cong {\frac{{8e} - {3{\left( {{\Delta \quad ɛ} - C} \right) \cdot \left( {1 + k_{p}} \right)}}}{\left( {{8e} - {3\left( {{\Delta ɛ} - C} \right)}} \right) \cdot \left( {1 - \frac{k_{p}}{k}} \right)}\quad {and}}$ ${{\Delta ɛ} = {{2C} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}};{and}$

b) calculating the pay saturation using the following equation: $S_{PAY} \cong {\frac{3 \cdot \left( {{\Delta ɛ} - C} \right) \cdot {kp}}{\left( {1 - \frac{kp}{kb}} \right) \cdot \left( {{8e} - {3\left( {{\Delta ɛ} - C} \right)}} \right)} - \frac{\frac{kp}{kb}}{1 - \frac{kp}{kb}}}$


7. The method of claim 4, further comprising the steps of: a) determining the water saturation by the following equations, $S_{w} \cong \frac{\begin{matrix} {{kb} \cdot \left( {{3 \cdot \left( {{\Delta\delta} - C} \right) \cdot \left( {g - 1} \right) \cdot \left( {{kp} + 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.} \\ \left. {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)}} \right) \end{matrix}}{\begin{matrix} {\left( {{kb} - {kp}} \right) \cdot \left( {{3 \cdot \left( {{\Delta\delta} - C} \right) \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.} \\ \left. {8 \cdot e \cdot \left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)} \right) \end{matrix}}$ and ${{\Delta\delta} = {{\frac{8}{g^{2}} \cdot A} + {2 \cdot B} - {\left( {1 + \frac{4}{g^{2}}} \right){dV}\quad \frac{\rho}{\overset{\_}{V\quad \rho}}} + \frac{8{dV}_{s}}{V_{s}}}};$

 and b) calculating the pay saturation using the following equation: S_(PAY)=1−S_(w).
 8. The method of claim 4, further comprising the steps of: a) determining the water saturation by the following equations, $S_{w} = \frac{{{kb} \cdot \left( {{\left( {{\Delta\delta} - C} \right) \cdot 135 \cdot {kp}} + 119} \right)} - {480 \cdot e}}{\left( {{kb} - {kp}} \right) \cdot \left( {{119 \cdot \left( {{\Delta\delta} - C} \right)} - {480 \cdot e}} \right)}$ and ${{\Delta\delta} = {{\frac{8}{g^{2}} \cdot A} + {2 \cdot B} - {\left( {1 + \frac{4}{g^{2}}} \right)\frac{{dV}\quad \rho}{\overset{\_}{V\quad \rho}}} + \frac{8{dV}_{s}}{V_{s}}}};{and}$

b) calculating the pay saturation using the following equation: S_(PAY)=1−S_(w).
 9. The method of claim 3, further comprising the following steps: a) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equations, AMP(θ)=B₀+B₁ TAN²θ+B₂ TAN²θ SIN²θ  Where: $B_{0} = {A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta\rho}{\rho}}}}$ $B_{1} = {B = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} - {\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta\rho}{\rho}} \right)} + {\frac{1}{2}{\Delta\delta}}}}$ $B_{2} = {{C - B} = {{\frac{2}{g^{2}}\left( {{2\frac{\Delta \quad {Vs}}{Vs}} + \frac{\Delta \quad \rho}{\rho}} \right)} + {\frac{1}{2}\Delta \quad ɛ} - {\frac{1}{2}\Delta \quad \delta}}}$

 and where: $g = \frac{\overset{\_}{Vp}}{\overset{\_}{Vs}}$ $\frac{\Delta \quad {Vp}}{\overset{\_}{Vp}} = \frac{{Vp}_{2} - {Vp}_{1}}{\overset{\_}{Vp}}$ $\frac{\Delta \quad {Vs}}{Vs} = \frac{{Vs}_{2} - {Vs}_{1}}{\overset{\_}{Vs}}$ $\frac{\Delta \quad \rho}{\rho} = \frac{\rho_{2} - \rho_{1}}{\overset{\_}{\rho}}$ Δδ = δ₂ − δ₁ Δɛ = ɛ₂ − ɛ₁ $\overset{\_}{Vp} = \frac{{Vp}_{1} + {Vp}_{2}}{2}$ $\overset{\_}{Vs} = \frac{{Vs}_{1} + {Vs}_{2}}{2}$ $\overset{\_}{\rho} = \frac{\rho_{1} + \rho_{2}}{2}$

 to generate curve shape parameters B₀, B₁, and ₂; and b) extracting rock property contrasts from the curve shape parameters using the following equations, $\frac{\Delta\rho}{\rho} = {{2\left( {B_{0} - B_{1} - B_{2}} \right)} + {\Delta ɛ}}$ $\frac{{\Delta \quad V\quad \rho}\quad}{V\quad \rho} = {{2\left( {B_{1} + B_{2}} \right)} - {\Delta ɛ}}$ $\frac{\Delta \quad {Vs}}{Vs} = {B_{0} - B_{1} - {B_{2}\left( {1 + \frac{g^{2}}{4}} \right)} + {\frac{g^{2}}{g}\left( {{\Delta ɛ} - {\Delta\delta}} \right)} + {\frac{1}{2}{\Delta ɛ}}}$ ${\Delta\delta} = {{\frac{8}{g^{2}}B_{0}} + {2B_{1}} - {\left( {1 + \frac{4}{g^{2}}} \right)\frac{{dV}\quad \rho}{\overset{\_}{V\quad \rho}}} + \frac{8{dV}_{s}}{g^{2}V_{s}}}$ ${\Delta ɛ} = {{2\left( {B_{1} + B_{2}} \right)} - {\frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}.}}$


10. The method of claim 9, further comprising the steps of: a) determining the water saturation by the following equation, ${S_{w} = \frac{\left( {{2B_{0}} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}};{and}$

b) calculating the pay saturation using the following equation: $S_{PAY} = {1 - {\frac{{2B_{0}} - \frac{\Delta \quad {Vp}}{Vp}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}}$


11. The method of claim 9, further comprising the steps of: a) determining the water saturation by the following equation, ${S_{w} \cong \frac{{8e} - {3{\left( {{\Delta ɛ} - C} \right) \cdot \left( {1 + k_{p}} \right)}}}{\left( {{8e} - {3\left( {{\Delta ɛ} - C} \right)}} \right) \cdot \left( {1 - \frac{k_{p}}{k}} \right)}};{and}$

b) calculating the pay saturation using the following equation: $S_{PAY} \cong {\frac{3 \cdot \left( {{\Delta ɛ} - C} \right) \cdot {kp}}{\left( {1 - \frac{kp}{kb}} \right) \cdot \left( {{8e} - {3\left( {{\Delta ɛ} - C} \right)}} \right)} - {\frac{\frac{kp}{kb}}{1 - \frac{kp}{kb}}.}}$


12. The method of claim 9, further comprising the steps of: a) determining the water saturation by the following equation, $S_{w} \cong \frac{\begin{matrix} {{kb} \cdot \left( {{3 \cdot \left( {{\Delta\delta} - C} \right) \cdot \left( {g - 1} \right) \cdot \left( {{kp} + 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.} \\ \left. {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)}} \right) \end{matrix}}{\begin{matrix} {\left( {{kb} - {kp}} \right) \cdot \left( {{3 \cdot \left( {{\Delta\delta} - C} \right) \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.} \\ \left. {8 \cdot e \cdot \left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)} \right) \end{matrix}}$

 and b) calculating the pay saturation using the following equation: S_(PAY)=1−S_(w).
 13. The method of claim 9, further comprising the steps of: a) determining the water saturation by the following equation, ${S_{w} = \frac{{{kb} \cdot \left( {{\left( {{\Delta\delta} - C} \right) \cdot 135 \cdot {kp}} + 119} \right)} - {480 \cdot e}}{\left( {{kb} - {kp}} \right) \cdot \left( {{119 \cdot \left( {{\Delta\delta} - C} \right)} - {480 \cdot e}} \right)}};{and}$

b) calculating the pay saturation using the following equation: S_(PAY)=1−S_(w).
 14. A method for determining pay saturation (S_(PAY)) of subsurface layers when a contact event is evident within the layers, comprising the following steps: a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint; b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface anisotropic layers, for each source-detector pair; c) sorting the traces into common midpoint (CMP) gathers, which have a common midpoint or reflection point, and have varying offsets; d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons; e) modifying the seismic data samples to generate velocity-corrected seismic data samples; f) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted amplitudes; and g) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample.
 15. The method of claim 14, further comprising the steps of: a) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equation, AMP=A+B SIN²θ+C(TAN²θ−SIN²θ)  Where: $A = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta \quad \rho}{\rho}}}$ $B = {\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}}$ $C = {\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}}$

 to generate curve shape parameters A, B and C; and b) extracting rock property contrasts from the curve shape parameters using the following equation, $\frac{\Delta\rho}{\rho} = {2\left( {A - B} \right)}$

c) determining the water saturation by the following equation, $S_{w} = \frac{2\left( {A - B} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}$

 where: A and B are the data derived curve fit coefficients; ρ_(PAY) is the density of pure pay in situ; ρ_(BR) is the density of pure brine in situ; {overscore (ρ)} is the average density if the brine and fluid filled reservoir; and φ is the porosity of the reservoir; and d) calculating the pay saturation using the following equation: $S_{PAY} = {1 - {\frac{2\left( {A - B} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}}$


16. The method of claim 14, further comprising the steps of: a) fitting the extracted amplitudes and the corresponding angles of incidence (θ), to the following equation, AMP=B₀+B₁ TAN²θ+B₂ TAN²θ* SIN²θ,  where: $B_{0} = {{\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}} + {\frac{1}{2}\frac{\Delta\rho}{\rho}}}$ $B_{1} = {\frac{1}{2}\frac{\Delta \quad {Vp}}{Vp}}$ B₂ = 0

 to generate curve shape parameters B₀, B₁ and B₂; b) extracting rock property contrasts from the curve shape parameters using the following equation, $\frac{\Delta\rho}{\rho} = {2\left( {B_{0} - B_{1}} \right)}$

c) determining the water saturation by the following equation, $S_{w} = \frac{2\left( {B_{0} - B_{1}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}$

 where: B₀ and B₁ are the data derived curve fit coefficients; ρ_(PAY) is the density of pure pay in situ; ρ_(BR) is the density of pure brine in situ; {overscore (ρ)} is the average density of the brine and fluid filled reservoir; and; φ is the porosity of the reservoir; and d) calculating the pay saturation using the following equation: $S_{PAY} = {1 - {\frac{2\left( {B_{0} - B_{1}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}}$


17. A method for determining pay saturation (S_(PAY)) of subsurface layers for P-P data, comprising the following steps: a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint; b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface anisotropic layers, for each source-detector pair; c) sorting the traces into common midpoint (CMP) gathers, which have a common midpoint or reflection point, and have varying offsets; d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons; e) modifying the seismic data samples to generate velocity-corrected seismic data samples; f) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample; g) angle stacking the seismic data samples through angle ranges θ_(s) and θ_(e); and h) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted angle stack amplitudes.
 18. The method of claim 17, further comprising the steps of: a) fitting the extracted angle stack amplitudes and the corresponding angles of incidence (θ), to the following equation, STACK(θ_(s),θ_(e))=A·f₁(θ_(s),θ_(e))+B·f₂(θ_(s),θ_(e))+C·f₃(θ_(s),θ_(e))  60  to generate AVO curve shape parameters A, B and C; and b) extracting rock property contrasts from the AVO curve shape parameters using the following equations, $\begin{matrix} {{\Delta\delta} = {{\frac{8}{g^{2}} \cdot A} + {2 \cdot B} - {\left( {1 + \frac{4}{g^{2}}} \right)\frac{{dV}\quad \rho}{\overset{\_}{V}\rho}} + {\frac{8}{g^{2}}\frac{{dV}_{s}}{\overset{\_}{V_{s}}}}}} & 68 \\ {{\Delta ɛ} = {{2C} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}} & 69 \\ {\frac{\Delta\rho}{\rho} = {{2\left( {A - C} \right)} + {\Delta ɛ}}} & 70 \end{matrix}$

c) determining the water saturation by the following equation, $\begin{matrix} {S_{w} = \frac{\left( {{2A} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & 75 \end{matrix}$

 Where: A and C are the data derived curve fit coefficients; ρ_(PAY) is the density of the pay fluid in situ; ρ_(BR) is the density of brine fluid in situ; {overscore (ρ)} is the average density of the fluid filled reservoir and the shale cap rock; φ is the porosity of the reservoir; and $\frac{\Delta \quad {Vp}}{Vp}$

is the velocity contrast; and d) calculating the pay saturation using the following equation: $\begin{matrix} {S_{PAY} = {1 - {\frac{{2A} - \frac{\Delta \quad {Vp}}{Vp}}{\varphi\left( \left( {\rho_{BR} - \rho_{BPAY}} \right) \right.}.}}} & 76 \end{matrix}$


19. The method of claim 17, further comprising the steps of: a) fitting the extracted angle stack amplitudes and the corresponding angles of incidence (θ), to the following equation, STACK(θ_(s),θ_(e))=B₀·G₁(θ_(s), θ_(e))+B₁·G₂(θ_(s), θ_(e))+B₂·G₃(θ_(sT), θ_(e))  64  to generate AVO curve shape parameters B₀, B₁ and B₂; and b) extracting rock property contrasts from the AVO curve shape parameters using the following equations, $\begin{matrix} {{\Delta \quad \delta} = {{\frac{8}{g^{2}}B_{0}} + {2B_{1}} - {\left( {1 + \frac{4}{g^{2}}} \right)d\quad V\quad \frac{\rho}{\overset{\_}{V}\quad \rho}} + {\frac{8}{g^{2}}d\quad \frac{V_{s}}{{\overset{\_}{V}}_{s}}}}} & 71 \\ {{\Delta \quad ɛ} = {{2\left( {B_{1} + B_{2}} \right)} - \frac{\Delta \quad V\quad \rho}{\overset{\_}{V\quad \rho}}}} & 72 \\ {{\frac{\Delta \quad \rho}{\rho} = {2\left( {B_{0} - B_{1} - B_{2}} \right)}};\quad {and}} & 73 \end{matrix}$

c) determining the water saturation by the following equation, $\begin{matrix} {S_{w} = \frac{\left( {{2B_{0}} - \frac{\Delta \quad {Vp}}{Vp}} \right)}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & 77 \end{matrix}$

 Where: B₀, B₁ and B₂ are the data derived curve fit coefficients; ρ_(PAY) is an estimate of the density of pay fluid in situ; ρ_(BR) is an estimate of the density of brine fluid in situ; {overscore (ρ)} is an estimate of the average density of the fluid filled reservoir and the cap rock; φ is an estimate of the porosity of the reservoir; and $\frac{\Delta \quad V\quad \rho}{V\quad \rho}$

is the velocity contrast; and d) calculating the pay saturation using the following equation: $\begin{matrix} {S_{PAY} = {1 - {\frac{{2B_{0}} - \frac{\Delta \quad {Vp}}{Vp}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}}} & 78 \end{matrix}$


20. The method of claim 17, further comprising the steps of: a) determining the water saturation by the following equation, $\begin{matrix} {S_{w} = \frac{{8\quad e} - {3{\left( {{\Delta \quad ɛ} - C} \right) \cdot \left( {1 + k_{p}} \right)}}}{\left( {{8\quad e} - {3\left( {{\Delta \quad ɛ} - C} \right)}} \right) \cdot \left( {1 + \frac{k_{p}}{k}} \right)}} & 85 \end{matrix}$

 and b) calculating the pay saturation using the following equation: $\begin{matrix} {S_{PAY} = {\frac{{3 \cdot \left( {{\Delta \quad ɛ} - C} \right) \cdot k}\quad p}{\left( {1 - \frac{k\quad p}{k\quad b}} \right) \cdot \left( {{8\quad e} - {3{\left( {\Delta \quad ɛ} \right) \cdot}}} \right)} - {\frac{\frac{k\quad p}{k\quad b}}{1 - \frac{k\quad p}{k\quad b}}.}}} & 86 \end{matrix}$


21. The method of claim 17, further comprising the step of determining the water saturation by the following equation: $\begin{matrix} {s_{w} = {\frac{\begin{matrix} {k\quad {b \cdot \left( {{3 \cdot {\Delta\delta} \cdot \left( {g - 1} \right) \cdot \left( {{k\quad p} + 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.}} \\ \left. {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)}} \right) \end{matrix}}{\begin{matrix} {\left( {{k\quad b} - {k\quad p}} \right) \cdot \left( {{3 \cdot {\Delta\delta} \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g^{2}} - 2} \right)} +} \right.} \\ \left. {8 \cdot e \cdot \left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} - {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)}} \right)} \right) \end{matrix}}.}} & 89 \end{matrix}$


22. The method of claim 17, further comprising the step of determining the water saturation by the following equation: $\begin{matrix} {S_{w} = {\frac{{k\quad {b \cdot \left( {{{\left( {{\Delta\delta} - C} \right) \cdot 135 \cdot k}\quad p} + 119} \right)}} - {480 \cdot e}}{\left( {{k\quad b} - {k\quad p}} \right) \cdot \left( {{119 \cdot \left( {{\Delta\delta} - C} \right)} - {480 \cdot e}} \right)}.}} & 91 \end{matrix}$


23. The method of claim 17, further comprising the steps of: a) fitting the extracted angle stack amplitudes and the corresponding angles of incidence (θ), to the following equation, STACK(θ_(s),θ_(e))=A·f₁(θ_(s), θ_(e))+B·f₂(θ_(s), θ_(e))+C·f₃(θ_(s), θ_(e))  92  where: $\begin{matrix} {f_{1} = 1} & 93 \\ {f_{2} = {\frac{1}{2}\left\lbrack {1 - \left( {\frac{{SIN}\quad \left( \theta_{e} \right){COS}\quad \left( \theta_{e} \right)}{\left( {\theta_{e} - \theta_{s}} \right)} - \frac{{SIN}\quad \left( \theta_{s} \right){COS}\quad \left( \theta_{s} \right)}{\left( {\theta_{e} - \theta_{s}} \right)}} \right)} \right\rbrack}} & 94 \\ \begin{matrix} {f_{3} = \quad {\frac{1}{2}\left\lbrack {{- 3} + \frac{{{TAN}\quad \left( \theta_{e} \right)} - {{TAN}\quad \left( \theta_{s} \right)}}{\left( {\theta_{e} - \theta_{s}} \right)} +} \right.}} \\ {\quad \left. \frac{{{SIN}\quad \left( \theta_{e} \right){COS}\quad \left( \theta_{e} \right)} - {{SIN}\quad \left( \theta_{s} \right){COS}\quad \left( \theta_{s} \right)}}{\left( {\theta_{e} - \theta_{s}} \right)} \right\rbrack} \end{matrix} & 95 \end{matrix}$

 to generate AVO curve shape parameters A, B and C; and b) extracting rock property contrasts from the AVO curve shape parameters using the following equations, $\begin{matrix} {{\Delta \quad \delta} = {\frac{\begin{matrix} {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} -} \right.}} \\ {\left. {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)} \right) \cdot \left( {k\quad {b \cdot \left( {s - 1} \right) \cdot k}\quad {p \cdot s}} \right)} \end{matrix}}{\begin{matrix} {3 \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g} - 2} \right) \cdot} \\ \left( {{k\quad {b \cdot \left( {{k\quad p} - s + 1} \right)}} + {k\quad {p \cdot s}}} \right) \end{matrix}} + C}} & 88 \\ {{\Delta \quad ɛ} = {\frac{8 \cdot {e\left( {{S_{w}\left\lbrack {k_{p} - k_{b}} \right\rbrack} + k_{b}} \right)}}{3\left( {{k_{b}\left( {k_{p} + 1} \right)} + {S\left( {k_{p} - k_{b}} \right)}} \right)} + C}} & 84 \\ {{{\frac{\Delta \quad \rho}{\rho} = {{2\left( {A - C} \right)} + {\Delta \quad ɛ}}}\quad;\quad {and}},} & 18 \end{matrix}$

c) determining the water saturation by the following equation, $\begin{matrix} {S_{w} = {\frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}} & 74 \end{matrix}$


24. The method of claim 17, further comprising the steps of: a) fitting the extracted angle stack amplitudes and the corresponding angles of incidence (θ), to the following equation, STACK(θ_(s),θ_(e))=B₀·G₁(θ_(s), θ_(e))+B₁·G₂(θ_(s), θ_(e))+B₂·G₃(θ_(sT), θ_(e))  96  where: G₁=1  97 $\begin{matrix} {G_{2} = \left\lbrack {{\frac{1}{\left( {\theta_{e} - \theta_{s}} \right)}\quad \left( {{{TAN}\quad \left( \theta_{e} \right)} - {{TAN}\quad \left( \theta_{s} \right)}} \right)} - 1} \right\rbrack} & 98 \\ \begin{matrix} {G_{3} = \quad \left\lbrack {{- \frac{3}{2}} + {\left( \frac{1}{\left( {\theta_{e} - \theta_{s}} \right)} \right)\left( {{{TAN}\quad \theta_{e}} - {{TAN}\quad \theta_{s}}} \right)} +} \right.} \\ {\quad \left. {\frac{1}{2}\left( \frac{1}{\theta_{e} - \theta_{s}} \right)\quad \left( {{{SIN}\quad \theta_{e}{COS}\quad \theta_{e}} - {{SIN}\quad \theta_{s}{COS}\quad \theta_{s}}} \right)} \right\rbrack} \end{matrix} & 99 \end{matrix}$

 to generate AVO curve shape parameters B₀, B₁ and B₂; and b) extracting rock property contrasts from the AVO curve shape parameters using the following equations, $\begin{matrix} {{\Delta \quad \delta} = {\frac{\begin{matrix} {8 \cdot {e\left( {{16 \cdot e \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right)} -} \right.}} \\ {\left. {13 \cdot \left( {{3 \cdot g^{2}} - 2} \right)} \right) \cdot \left( {k\quad {b \cdot \left( {s - 1} \right) \cdot k}\quad {p \cdot s}} \right)} \end{matrix}}{\begin{matrix} {3 \cdot \left( {g - 1} \right) \cdot \left( {{9 \cdot g} + 17} \right) \cdot \left( {{3 \cdot g} - 2} \right) \cdot} \\ \left( {{k\quad {b \cdot \left( {{k\quad p} - s + 1} \right)}} + {k\quad {p \cdot s}}} \right) \end{matrix}} + C}} & 88 \\ {{\Delta \quad ɛ} = {\frac{8 \cdot {e\left( {{S_{w}\left\lbrack {k_{p} - k_{b}} \right\rbrack} + k_{b}} \right)}}{3\left( {{k_{b}\left( {k_{p} + 1} \right)} + {S\left( {k_{p} - k_{b}} \right)}} \right)} + C}} & 84 \\ {{{{\left. c \right)\quad \frac{\Delta \quad \rho}{\rho}} = {{2\left( {A - C} \right)} + {\Delta \quad ɛ}}}\quad;\quad {and}},} & 18 \end{matrix}$

d) determining the water saturation by the following equation, $\begin{matrix} {S_{w} = {\frac{\Delta \quad \rho}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}} & 74 \end{matrix}$


25. A method to determine pay saturation (S_(PAY)) of subsurface layers for P-S data, comprising the following steps: a) positioning and employing a plurality of seismic wave source-detector pairs having different offsets and one common horizontal midpoint; b) generating seismic waves with the source-detector pairs, and detecting and recording into traces, as seismic data samples, the amplitudes of seismic waves reflected by discontinuities in the subsurface anisotropic layers, for each source-detector pair; c) sorting the traces into common reflection point (CRP) gathers, which have a common reflection point, and have varying offsets; d) providing amplitude corrections to the seismic data samples to eliminate effects associated with spherical divergence, array effects, transmission effects, absorption effects, and other effects associated with energy propagating through and reflecting from subsurface horizons; e) modifying the seismic data samples to generate velocity-corrected seismic data samples; f) calculating the angle of incidence (θ) by using a velocity function and source receiver separations, for each seismic data sample; and g) extracting amplitudes from the seismic data samples, for each subsurface horizon, to generate extracted amplitudes.
 26. The method of claim 25, further comprising the steps of: a) fitting the extracted angle stack amplitudes and the corresponding angles of incidence (θ), to the following equation, $\begin{matrix} \begin{matrix} {{{AMP\_ PS}(\theta)} = \quad {{D_{0}\left( {\frac{{SIN}\quad {\theta \left( {{{SIN}^{2}\quad \theta} - g^{2}} \right)}}{2g\sqrt{g^{2} - {{SIN}^{2}\quad \theta}}} - \frac{{SIN}\quad {\theta COS}\quad \theta}{g}} \right)} +}} \\ {\quad {D_{1}\left( {\frac{2{SIN}^{3}\quad \theta}{g\sqrt{g^{2} - {{SIN}^{2}\quad \theta}}} - \frac{2{SIN}\quad {\theta COS}\quad \theta}{g}} \right)}} \end{matrix} & 104 \end{matrix}$

 where $\begin{matrix} {D_{0} = \frac{\Delta \quad \rho}{\overset{\_}{\rho}}} & 105 \\ {D_{1} = \frac{\Delta \quad {Vs}}{\overset{\_}{Vs}}} & 106 \end{matrix}$

b) calculating the water saturation using the following equation: $\begin{matrix} {S_{w} = \frac{{\Delta \quad \rho_{PS}} - {\Delta \quad \rho_{BR}}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}} & 109 \end{matrix}$

Where: Δρ_(PS)=ρ_(PS)−ρ_(SHALE); ρ_(BS)=ρ_(BS)−ρ_(SHALE); ρ_(FLUID)=Density of the fluid filling the pore space φ—the fluid has water saturation S_(w); ρ_(BR)=Density of the brine; ρ_(PAY)=Density of the pure pay; φ=Porosity of the reservoir; ρ_(PS)=Density of pay filled layer of saturation S_(w); and ρ_(PS)=Density of brine filled layer; and c) calculating the pay saturation using the following equation: $\begin{matrix} {S_{PAY} = {{1 - S_{w}} = {1 - {\frac{\left( {D_{0_{B}} - D_{0_{A}}} \right)\overset{\_}{\rho}}{\varphi \left( {\rho_{BR} - \rho_{PAY}} \right)}.}}}} & 114 \end{matrix}$ 